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GEOLOGICAL SURVEY OF ALABAMA 

EUGENE ALLEN SMITH, State Geologist 

The 

Underground Water Resources 

of Alabama 



By 
EUGENE ALLEN SMITH 



PREPARED IN CO-OPERATION WITH THE UNITED STATES 
GEOLOGICAL SURVEY 




Montgomery, Alabama 

The Brown Printing Company, State Printers and Binders 

1907 



D« of D. 






3 



V 

o3 PREFATORY LETTER. 



To lu's Excellency, 

B. B." Comer, 

Governor of Alabama, 

Sir: — Since 1898 th|e Geological Survey of Alabama in 
co-operation with the United States Geological Survey, has 
been engaged in the systematic investigation of the Water 
Resources of the State. 

Most of the well records contained in the present report were 
published by the United States Geological Survey, in Water 
Supply and Irrigation Paper Xo. 102, "Contributions to die 
Hydrology of the Eastern United States, by M. L. Fuller, 
1903-4." A year later a Summary of the Underground Water 
Conditions in Alabama, with a sketch map showing approxi- 
mately the artesian water systems of the State, was prepared 
by the present writer for Water Supply and Irrigation Paper 
No. 114 of the National Survey, "Underground Water Condi- 
tions of the Eastern United States, by M. L. Fuller, 1904." 

The manuscript of this report, in approximately its present 
form, was submitted in July 1905 to the Director of the United 
States Geological Survey. In that office it was edited, to its 
material improvement, and with the expectation of earlv publi- 
cation ; but owing to the congestion of work at the Govern- 
ment Printing Office, the prospect of immediate publication by 
the National Survey seemed to be so remote that the manu- 
script was returned for publication by the Alabama Survey. 

During this interval a considerable amount of new material 
had accumulated, which has been incorporated in the report, 
together with additional sections in the discussion of the Chem- 
istn and Classification of the Alabama Waters. 

I trust that the report now submitted to the people of Ala- 
bama may be of service to many, and that in due time it may 
be followed by a more comprehensive account of the Under- 
ground Water Resources of the State, and especially of the 
medicinal waters'. 



IV PREFATORY LETTER. 

Most of the records of wells and springs herein mentioned 
were collected by Dr. B. F. Lovelace, then with the University 
of Alabama ; some, by Mr. James A. Anderson of Alabama Sur- 
vey ; the rest by correspondence from the office of the United 
States' Geological Survey. The analyses, with the few excep- 
tions duly credited, were made in the laboratory of the Ala- 
bama Survey by Mr. R. S. Hodges, Chemist to the Survey. 
Very respectfully, 

Eugene A. Smith, 

State Geologist. 

University of Alabama, March 25, 1907. 



TABLE OF CONTENTS. 

CHAPTER I. 

Physical Geography, Geology and Climate ] 

Physical geography and natural divisions 1 

Geographic position 1 

Surface configuration and grand divisions 1 

River systems 2 

Mountain and table-lands 3 

Subdivisions <s 

Geology 4 

Appalachian division 6 

Talladega Mountains and Ashland Plateau 6 

Appalachian Valleys 7 

Coal Fields 9 

Valley of the Tennessee 10 

Coastal Plain division 12 

Cretaceous 13 

Tuscaloosa formation 18 

Eutaw sands 13 

Selma chalk 13 

Ripley formation 13 

Tertiary 14 

Eocene 14 

Midway group 15 

Clayton limestone 15 

Sucarnochee clay 15 

Naheola (Matthews Landing) formation 15 

Chickasaw (Wilcox) group- 15 

Nanafalia formation (Coal Bluff) 16 

Tuscahoma formation (Bells Landing) 17 

Bashi formation (Woods Bluff) ; 17 

Hatchetigbee formation 17 

Claiborne group 17 

Tallahatta buhrstone 17 

Lisbon formation 18 

Gosport greensand 18 

St. Stephens Limestone 19 

Topographic features of the Eocene 19 

Miocene 21 

Chattahoochee series 21 

Pliocene 21 

Pascagoula 21 

Grand Gulf formation 22 

Quaternary 24 

Lafayette formation 24 

Later formations 25 

Climate of Alabama, by Frank P. Chaffee 25 

General features 25 

Temperature 26 

Killing frost 26 

Precipitation 28 

Hail 29 

Fog 29 

Thunderstorms 29 

Winds 30 



vi TABLE OF CONTENTS. 

CHAPTER II. 

A. General discussion of underground waters 32 

Source of circulating waters 32 

Disposition of the water falling upon the land surface 32 

Evaporation before absorption 33 

Direct runoff or flood-flow . 33 

Absorption 34 

Final runoff 35 

Amount of water available to artesian wells 35 

Depth of penetration 36 

Distribution and movements of underground waters 37 

Modifications of groundwater movement due to physical 

structure 37 

Porosity 37 

Amount of water absorbed by porous rocks 38 

Incomplete saturation 39 

Lost water '. 39 

Permeability 40 

Cause and rate of movement of underground waters 40 

Velocity ! 41 

Flow or discharge 41 

Modifications of groundwater movement due to topography 43 

Groundwater divisions 43 

Surface zone of flow 44 

Form of the groundwater table 44 

Modifications of groundwater movement due to stratifica- 
tion 46 

Deep zones of flow 46 

Recovery of underground waters 48 

Waters near the surface 48 

Springs 48 

Open wells 49 

Driven wells . 49 

Deep-seated waters 51 

Deep springs (Fissure springs) 51 

Artesian wells 51 

B. Artesian Wells 52 

Essential conditions 52 

Artesian system ! 53 

Modifying conditions 57 

Effects of erosion 57 

Variations in the water-bearing stratum 58 

Variations in the confining impervious beds 59 

Other modifying conditions 60 

Arrangement of the strata in the Alabama Coastal Plain 61 

Decline or failure of artesian wells 62 

Increase of leakage 62 

Closure of the bore . 62 

Decline from exhaustion 62 

Character of the water 63 

Temperature ■ 63 

Mineral ingredients 64 

CHAPTER III. 

Detailed description of the Underground waters of Alabama. 

Appalachian division 66 

Talladega Mountains and Ashland Plateau__: 66 



TABLE OF CONTENTS. vn 

Surface features 66 

shallow waters 66 

.Mineral waters 67 

Artesian prospects 68 

Lanett wells 70 

Alexander City wells 711 

Auburn, Lee county 71 

Appalachian Valleys 71 

Surface features 71 

Shallow waters 71 

Mineral waters 72 

Sulphur and chalybeate waters 73 

Jones springs 73 

St. Clair springs 73 

Talladega springs 74 

Shelby springs 75 

Hawkins well — Leeds mineral water 75 

Alabama White Sulphur springs 76 

Blount springs and vicinity 77 

Cold spring 79 

Glenwood Springs 79 

HarrelPs well 80 

Borden- Wheeler springs 80 

Other springs 81 

Ingram Well 82 

Saline Waters 82 

Landers well and Gary springs 82 

Ball Flat well 83 

Artesian prospects 84 

Anniston 85 

<Jate City 86 

Coal Measures (Carboniferous rocks) : 88 

Shallow waters 88 

Mineral waters 88 

Cook springs 89 

Springs on Shades Mountain : . 89 

Springs on Lookout Mountain 90 

Mentone springs 91 

Other springs _: 91 

Artesian prospects 1)2 

Etowah county 93 

Cahaba field 94 

St. Clair County !>4 

Warrior field 94 

Walker County 94 

Cullman County 95 

Marion County 96 

Jefferson County 96 

Fayette County 97 

Tuscaloosa County !>7 

Valley of tbe Tennessee 100 

Surface features 100 

Shallow waters 100 

Mineral waters . 101 

Chalybeate springs 101 

Sulphur springs 101 

Alkaline-Saline springs 103 

Acid springs 104 

Tar spring's .. 104 

Artesian prospects 105 



TABLE OF CONTENTS. 

New Market 105 

Hazel Green ^ 106 

South of Tennessee River 106 

Coastal Plain Division ' 108 

General account 108 

Waters of the Cretaceous • 111 

Tonibigbee-Alabaina-Conecuh rivers drainage 111 

Discussion by counties 113 

Lamar County ■. 113 

Shallow waters 113 

Artesian prospects 114 

Sulligent 114 

Fayette County 114 

Tuscaloosa County 115 

Surface features 115 

Shallow waters 115 

Artesian prospects 117 

Tuscaloosa and. vicinity 118 

Right bank of river 120 

Hulls 121 

Willifords 122 

Bibb County _ 122 

Chilton County 123 

Pickens County 123 

Surface features 123 

Shallow waters 123 

Artesian prospects 124 

Wells in the Eutaw formation 124 

Sipsey River 125 

Lubbub Creek 125 

Aliceville and vicinity 125 

Near Tombigbee River 126 

Pickensville and vicinity '. 127 

Wells in the Selma Chalk 12S 

Vienna and vicinity 128 

Stone and vicinity 129 

Sherman, Dancy and vicinity 130 

Sumter County 131 

Surface features 131 

Shallow waters ' 131 

Springs in Selma chalk 131 

Near Epes J 131 

Springs in the Tertiary foramtion 132 

York and vicinity 133 

Artesian prospects 135 

Warsaw and vicinity 135 

Gainesville and vicinity 137 

Epes and vicinity _ 139 

Sumterville and vicinity 141 

Livingston and vicinity 141 

Greene County 143 

Surface features • 143 

Artesian records 145 

Judge Mobley's list 146 

Sipsey 152 

Lock 6 now Lock 9, Black Warrior River__ 152 

Steeles Bluff 152 

Clinton and vicinity . 152 

Eutaw and vicinity and southward 152 

Hairston _: : 156 



TABLE OF CONTENTS. IX 

Boligee and vicinity 156 

Burton Hill 157 

Erie and vicinity 157 

Forkland and vicinity 157 

Bale County 158 

Surface features 158 

Artesian wells 158 

Moundville and vicinity 159 

Powers Station and vicinity 160 

Cypress Switch 160 

Stewarts and vicinity 160 

Akron and vicinity ]61 

Evans Station and vicinity 162 

Wedgworth, (Greenwood, Mays Station) 163 

Lock 4 (now Lock 7) 165 

Sawyerville and vicinity 166 

Erie . 166 

Greensboro and vicinity ' 167 

Millwood and vicinity 168 

Cedarville and vicinity 169 

Whitsitt and vicinity 170 

Newberne and vicinity 171 

Sunshine 174 

Laneville and vicinity . 174 

Gallion and vicinity 174 

Fannsdale and vicinity 175 

Perry County ■ 176 

Shallow waters 177 

Artesian waters 177 

Wells in the Tuscaloosa formation 177 

vTells in the Entaw formation 178 

Marion and vicinity 178 

Old Hamburg 178 

Radfordville 178 

Felix and vicinity 179 

Wells in the ^eluia chalk 180 

Uniontown and vicinity 180 

Scott's Station 180 

Southward from Marion 180 

Hamburg Station and vicinity 181 

Marion Junction and vicinity 1S2 

Marengo County 182 

Surface features 182 

Artesian records 183 

Demopolis and vicinity 183 

Gallion and vicinity 185 

Fannsdale and vicinity 185 

Near Old Spring Hill 186 

Dayton 186 

Linden 187 

Flatwoods or Post Oaks 188 

Lower part of the county 190 

Dallas County 190 

General Conditions 190 

Artesian records 192 

Cahaba 192 

Selma and vicinity 194 

Along the Louisville & Nashville R. R 199 

Orrville and vicinity 199 



TABLE OF CONTENTS. 

Martins Station and vicinity, Louisville & 

Nashville R. R. 109 

Near lines of Southern R. R. 200 

East of Alabama River 205 

Lowndes County '. 205 

Surface features . 206 

Artesian records 207 

Scott Hill 207 

Lowndes Station 207 

Corrie 207 

Hayneville 208 

Montgomery County 20S 

Surface features 208 

Shallow waters 208 

Artesian records '. 208 

Montgomery 209 

North and west of Montgomery 213 

South and east of Montgomery 213 

Autauga County 215 

Shallow waters 215 

Artesian prospects 215 

Prattville _ 215 

Autaugaville 219 

Elmore County 219 

Surface features 219 

Shallow waters 219 

Artesian conditions 220 

Prattville Junction 220 

Grandview 221 

State Farm 221 

Macon County , 221 

Surface features 221 

Artesian prospects 221 

Tuskegee 222 

Warriorstand 222 

Chesson 222 

Hardaway 222 

Downs and vicinity '. 222 

Fort Davis 223 

Roba 223 

Lee County 223 

Surface features 223 

Artesian prospects 223 

Auburn 223 

Girard 224 

Pike County '224 

Artesian prospects • '. 224 

Orion and vicinity 224 

Logton 225 

Linwood 225 

Troy 225 

Bullock County 226 

Surface features 226 

Artesian prospects . 227 

Mitchell Station 227 

Fitzpatrick 227 

Thompson Station 227 

North of Chunnennugga Ridge 227 

Shopton and vicinity '. 227 

Bughall 228 



TABLE OF CONTENTS. xi 

Union Springs and vicinity 228 

Easi of Union Springs 2i".> 

Smith of Union Springs 229 

Chattahoochee River drainage — "blue marl region" 230 

Stratigraphic characters 230 

Countv details L 232 

Russell county 232 

Surface features 232 

Artesian records 232 

Kaolin Station 232 

Hurtsboro and vicinity 233 

Hatchechubbee and vicinity 234 

Scale and vicinity 234 

Rutherford and vicinity 235 

Pittsboro and vicinity \ 236 

Glenville and vicinity 237 

Barbour County 238 

Surface features 238 

Artesian prospects 240 

Eufaula and vicinity 240 

Harris and vicinity 242 

Clayton 244 

Waters of the Tertiary , 245 

General statement 245 

Discussion by counties 252 

Henry County 252 

Surface features 252 

Artesian record . 252 

Houston County 252 

Surface features 252 

Artesian records 253 

Columbia 253 

Dothan 253 

Geneva County 2."4 

Surface features 254 

Artesian records . 254 

Geneva 2o4 

Hartford _.>*> 

Slocomb 255 

Dale County . 255 

Artesian prospects 2\55 

Ozark 256 

Coffee County 256 

Surface features 256 

Artesian prospects 256 

Elba and vicinity 257 

Brocton 257 

Enterprise — 25S 

Covington County 258 

Surface features 258 

Shallow waters 258 

Artesian prospeets 259 

Andalusia and vicinity 259 

River Falls and Sauford 260 

Crenshaw County 2iU 

Surface features 261 

Artesian prospects 261 

Theba 262 

Brantley and vicinity 262 

Searigbt ' 263 



TABLE OF CONTENTS. 

Butler County 263 

Surface features . 263 

Mineral waters 263 

Roper's well 263 

Butler Springs 265 

Artesian prospects 266 

Greenville 266 

Forest 266 

Boiling 266 

Chapman 267 

Dunham 267 

Conecuh County '. ■ 267 

Surface features 267 

Artesian prospects 268 

Evergreen 268 

Escambia County 268 

Surface features 268 

Artesian prospects 269 

Brewton and vicinity 269 

Herrington and vicinity 271 

Pollard 271 

West of Pollard 272 

Roberts 273 

Monroe County 276 

Surface features 276 

Mineral waters 276 

Awin and vicinity 276 

' Tunnel Springs 277 

Artesian prospects 277 

Nadawah 278 

Maros 278 

Wilcox County 279 

Surface features 279 

Mineral waters 280 

Caledonia 280 

Schuster 280 

Awin 281 

Other Springs 281 

Artesian prospects 282 

Pine Hill • 282 

Catherine and Ancinity , 282 

Clarke County 283 

Surface features 283 

Mineral waters 283 

Tallahatta Springs 283 

Lower Salt Works Sulphur Springs 283 

Artesian prospects 284 

Old Salt wells 284 

Recent borings 286 

Choctaw County 290 

Surface features 290 

Mineral Springs 290 

Springs of the Claiborne formation 290 

Thornton springs 290 

Mineral extracts '. 290 

Springs of the Buhrstone and Hatchetigbee 

formations 291 

Bladon Springs 291 

Springs along Turkey Creek 293 

Other Springs . 293 



TABLE OF CONTENTS. xm 

Springs of the Woods Bluff formation 294 

Butler and vicinity 294 

Springs of the Tuscahoma formation 294 

Springs of the Nanafalia formation 294 

Springs of the Naheola formation 295 

Artesian prospects 295 

Cullum Springs 295 

Butler 297 

Washington County 297 

Surface features 297 

Mineral Springs 298 

Springs of the Hatchetigbee formation 298 

Springs of the Grand Gulf formation 299 

Healing Springs 299 

Artesian prospects 300 

Old Salt wells 300 

St. Stephens 301 

Mobile County 302 

Surface features 302 

Mineral waters 304 

Citronelle 304 

Springs near the coast 304 

Springs about Mobile Bay 306 

Artesian prospects 307 

Mobile and vicinity 307 

Alabama Port 311 

Fort Gaines 309 

Wells on Portersville Bay Shore 313 

Citronelle 314 

Baldwin County 314 

Surface features 314 

Shallow waters 315 

Mineral waters 316 

Artesian prospects 316 

Supplementary notes *. 317 

Additions 317 

Appalachian Valleys 317 

Valley of the Tennessee 317 

Coastal Plain Division 318 

Cretaceous 318 

Hale County 318 

Tertiary 320 

Sumter County 320 

Corrections. 

CHAPTER IV. 

Chemistrv and Classification of Alabama Waters 323 

Chemistry 323 

Classification 326 

Scheme of Classification 328 

Alkaline Waters (Tables I and II) 328 

Alkaline-Saline waters (Table III) 331 

Saline waters (Table IV) 332 

Acid waters (Table V) 334 

Generalizations 336 

Waters from the Tuscaloosa strata (Table VI) 336 

Waters from the Eutaw sands (Table VII) 337 

Waters from Upper Cretaceous and Tertiary strata 

(Table VIII) 338 



xiv TABLE OF CONTENTS. 

Blue Marl waters 338 

Tertiary waters 339 

Concluding Remarks 344 

Sanitary Analysis ■_. 345 

Analysis of Mineral Waters 346 

Tables of analyses of Alabama waters 351 

Table I. Calcic alkaline bi-carbonates waters 352-353 

Table II. Sodic alkaline bi-carbonated waters 354 

Table III. Alkaline-saline waters 356-357 

Table IV. Saline waters 358-359 

Table V. Acid waters 360 

Table VI. Waters derived from Tuscaloosa strata 361 

Table VII. Waters derived from Eutaw sands 362 

Table VIII. Waters derived from upper Cretaceous (Blue 

Marl) and Tertiary strata 363 



ILLUSTRATIONS. 

FULL PAGE PLATES. 

Plate I Frontispiece. 

Geological and Artesian Water Map of Alabama. 

Facing Page. 

Plate II — 49 

, Big Spring in Huntsville, Madison County. 
Plate III 74 

Talladega Springs, Talladega County. 
Plate IV 75 

Sbelby Springs, Shelby County. 
Plate V ____ 76 

Hawkins Well, (Leeds Mineral Water) Jefferson County. 
Plate VI , 77 

Alabama White Sulphur Springs, Dekalb County. 
Plate VII 78 

Blount Springs, Blount County. 
Plate VIII 80 

Borden- Wheeler Springs, Cleburne County. 
Plate IX ____ _ 82 

A. Ingram Well, near Ohatchee, Calhoun County. 

B. Gate City Well, Jefferson County. 

Plate X. 89 

A. Cook Springs, St. Clair County. 

B. Mentone Springs, Dekalb County. 

Plate XI ____ __ 100 

Big Spring, Tuscumbia, Colbert County. 
Plate XII ■— : 103 

Bailey Springs, Lauderdale County. 
Plate XIII _110-111 

Map of Alabama Showing Approximately the Artesian 
Systems. 
Plate XIV — 122 

Artesian Well at Willifords, Tuscaloosa County. 
Plate XV 169 

A. Well on Crassdale Plantation (J. O. Banks) near 
Eutaw Greene County. 

B.Pickens Well, near Greensboro, Hale County. 
Plate XVI 1--L _ ______ 197 



TABLE OF CONTENTS. xv 

A. Well in Elkdale Park, Selma, Dallas County. 

B. Old Road Showing Grand Gulf Strata capped with 
Lafayette near Gainestown Ferry, Clarke County. 

Plate XVII 246 

A. Blue Pond — Near Dixie. Covington County. 

B. Pavilion of Sulphur Well, near Clarke County. 

Plate XVIII 247 

Red Bluff on Mobile Bay near Montrose, Baldwin Coun- 
ty, Grand Gulf Strata capped with Lafayette. 
Plate XIX 248 

Bluff of Grand Gulf Strata overlain by Lafayette, 

Perdido Bay, near Soldiers Creek, Baldwin County. 

Plate XX 249 

Perdido Bay from Bluff, near Lillian, Baldwin County. 
Plate XXI ., 250 

Gum Pond. Flatwoods (Grand Gulf), Baldwin County. 
Plate XXII 251 

Pine Meadow or Savannah, between Swift and Lillian, 
Baldwin County. 
Plate XXIII 259 

MeDade's Pond, Florala, Covington County. 
Plate XXIV 292 

A. Hotel at Bladon Springs. Choctaw County. 

B. Pavilion of Sulphur Spring, Bladon Springs, Choc- 
taw County. 

Plate XXV 295 

Hotel at Culloni Springs near Bladon Springs, Choctaw 
County. 

Plate XXVI 297 

Salt Well at Culloni Springs, Choctaw County. 

Plate XXVII 299 

A. Mound Spring at Healing Springs, Washington 
County. 

B. Creek Spring at Healing Springs, Washington 
County. 

Plate XXVIII 310 

Bascomb Well No. 2 (Salt Water and Inflammable Gas), 
near Mobile, Mobile County. 

Plate XXIX 313 

Artesian Well, Oyster Canning Establishment, near 
Bavou LaBatre, Mobile County. 

Plate XXX 342 

Sketch Map of Cretaceous Formation. 



xvi TABLE OF CONTENTS. 

FIGURES IN TEXT. 

Fig. Page. 

1. Map showing mean annual temperatures in Alabama— 28 

2. Map showing average annual precipitation for Alabama 30 

3. Ideal section across a river valley showing the position of 

the groundwater, etc 45 

4. Diagrammatic section illustrating seepage and the growth 

of streams 45 

5. Hillside spring from unconfined water bed without head 48 

6. Hillside spring from confined bed under more or less head 49 

7. Diagram showing buried sloughs 50 

8. Fissure Spring 51 

9. Section showing conditions furnishing flows from unconfined 

sandy strata 1 ' . 53 

11. Diagrammatic representation of a single artesian system 54 

10. Ideal Artesian Basin 54 

12. Underground conditions in Thompsonville well (Conn.) 55 

13. Illustrating the influence of the dip of the strata on the 

width of the outcrop 55 

14. Section showing effects of erosion 58 

15. Section illustrating the thinning out of a porous water 

bearing bed : 58 

16. Section illustrating the transition of a porous water-bearing 

bed into a close textured impervious one 59 

17. Illustrating the overlapping of the intake area of the porous 

bed by an impervious bed 60 

18. Illustrating occurrence of a gravel bed completely enclosed 

in clays 6*0 

19. Illustrating occurrence of gravelly beds of ancient streams 

between impervious beds 60 

20. Illustrates conditions apparently favorable for water, but 

where it does not accumulate _ 61 

21. Section North and South across Alabama Coastal Plain 

illustrating its artesian conditions 62 

22. Well in jointed rock 69 

23. Diagram of Blount Springs 7S 



UNDERGROUND WATER RESOURCES 
OF ALABAMA. 



CHAPTER I. 

PHYSICAL GEOGRAPHY, GEOLOGY, AND CLIMATE. 



PHYSICAL GEOGRAPHY AND NATURAL DIVISIONS. 

Geographic position. — Alabama is situated between the 
eighty-fifth and eighty-ninth meridians of west longitude and 
mainly between the thirty-first and thirty-fifth parallels of north 
latitude. The total area thus included is, according to the latest 
estimates, 52,251 square miles, of which 51,540 square miles' 
constitute the land surface. 

Surface Configuration and Grand Divisions. — Apart from the 
minor inequalities and the relatively small area of the Talladega 
Mountains, the surface of the State may be considered as an 
eroded or dissected plain, whose mean elevation above sea 
level is not much less than 600 feet. To the north and east the 
surface rises above this elevation and to the south and west it 
sinks below it. A curving line drawn from the northwest cor- 
ner of the State through Tuscaloosa and Montgomery to Co- 
lumbus, Georgia, would mark approximately the southern 
boundary of the area whose altitude is above 600 feet. This 
elevated land is the Southwestern terminus of the great Appa- 
lachian region, and forms' the Appalachian Division of this 
report. 

The line along which the highest altitudes occur — i. e., the 
axis of elevation of this area — runs in a northeast-southwest 
direction nearly along the northern boundaries of Coosa, Clay, 
and Cleburne counties. The altitude increases toward the 
northeast, and as a consequence the general slope of the surface 
is away from this elevated area toward die northwest, west, 



2 PHYSICAL GEOGRAPHY, GEOLOGY AND CLIMATE. 

southwest, south, and southeast. The mountains of the State 
all rise 1200 to 1600 feet above the highland, or 2000 to 2400 
feet above sea level. The rest of the State, whose general alti- 
tude is less than 600 feet, constitutes the Coastal Plain Divi- 
sion. The surface of this' area slopes, approximately one foot 
to the mile, south and west toward the Gulf of Mexico and the 
Mississippi Valley. The elevation decreases from about 600 
feet where it touches the Appalachian division to 200 to 300 feet 
in the highlands overlooking the Gulf in the two coast counties. 
Into the materials of this gently sloping plain the rivers and 
other streams' have sunk their channels, leaving between them 
the remnants of the original mass which constitute the hills 
of this section of the State. 

Another point of difference between the two great divisions, 
readily seen by an inspection of the map, is the prevailing north- 
east-southwest direction of the minor subdivisions of the Appa- 
lachian area and the approximately east-west trend of such sub- 
divisions in the Coastal Plain area. Some other important dif- 
ferences between the two sections will be discussed below. 

River systems. — In general terms, two factors have been 
mainly instrumental in determining the direction of the drain- 
age systems of Alabama. These are, first, the slopes toward the 
northwest and southeast away from the Appalachian axis of 
elevation, and second, the more general slope of the surface of 
the State, taken as a whole, southwestward toward the Mis- 
sissippi Valley. The latter factor has greatly outweighed the 
former in fixing the direction of the watercourses, the result 
being that the whole drainage system of the State has a gen- 
eral southwesterly direction, with the single exception of the 
Tennessee River. 

In the southeastern half of the Appalachian area, while the 
natural fall is to the southeast and south, most of the streams, 
especially the minor ones, are also influenced by the northeast- 
southwest trend of the valleys and ridges and make their way 
toward the Coastal Plain in a zigzag course, alternating between 
southeast and southwest. In the northwestern half of the Ap- 
palachian area, the two branches of Black Warrior River fol- 
low in general the troughs or basins of the Warrior coal field, 
which pitch toward the southwest, while the Tennessee, en- 
tering the State near its northeastern corner, follows a limestone 



PHYSICAL GEOGRAPHY AND NATURAL DIVISIONS. 3 

valley southwestward to Guntersville, and then turns north- 
westward down the slope from the axis of the Appalachian 
highlands. 

In the central part of the Appalachian area the dependence 
of minor ridges and valleys on the geologic structure is most 
clearly seen. They all have a northeast-southwest trend, par- 
allel to the strike of the outcropping edges of the folded strata. 
The valleys are cut into the limestones and other easily eroded 
rocks, while the harder rocks form the ridges. 

In the Coastal Plain area the main or trunk streams have 
southerly or southwesterly courses, determined by the general 
slope of the surface ; while their minor tributaries together with 
attendant ridges and valleys, are controlled in location and di- 
rection by the geologic structure and by the character of the 
materials of the geological formations. 

Throughout the Coastal Plain the constituent beds of sand, 
clay, limestone, and marl, have a dip in the same general di- 
rection as the surface of the country, but at a more rapid rate — ■ 
on an average about 35 or 40 feet to the mile. While the main 
(consequent) streams' have cut across the edges of these slightly 
inclined beds, the smaller streams run roughly parallel to them. 
The result is that the landward or in-facing slopes of the minor 
stream valleys are abrupt, while the slopes facing gulfward are 
very gentle, often hardly to be distinguished from horizontal. 
Thus, while the adjustment of the smaller streams of the Coas- 
tal Plain to the geologic structure is not so striking, it is in 
places quite as complete as in the Appalachian area. 

Mountains and table-lands. — As has been intimated above, the 
mountainous region of the State is confined to the Appalachian 
division, the two halves of which (divided by a northeast- 
southwest line) show important differences. In the southeas- 
tern half the strata have been greatly folded and plicated and 
in part metamorphosed, and are always much indurated. As 
a consequence the mountains of this section, illustrated by the 
Talladega Mountain range, the most elevated in the State, are 
often sharp-crested and serrated, but always with uneven sum- 
mits. In the northwestern half the strata are in wide, open 
waves or folds, and the mountains, exemplified by the Cumber- 
land Plateau, are merel ythe remnants of an elevated table- 
land, with steep slopes toward the bordering valleys. Between 



4 PHYSICAL GEOGRAPHY, GEOLOGY AND CLIMATE. 

the principal members of this mountain system are great val- 
leys which are carved in the main from limestones interstrati- 
fied with harder and more durable beds' of sandstone and chert. 
These harder beds form northeast-southwest minor ridges 
which flute the great valley areas. 

There are no mountains properly so called in the Cqastal 
Plain. The hills, like those of the Cumberland Plateau, are 
merely remnants carved from the original mass. 

Sub-Divisions. — The sub-divisions' of the Appalachian area, 
based on the topographic and geologic features, are : ( I ) The 
Talladega Mountains and Ashland Plateau, of igneous and 
metamorphic rocks; (2) the Appalachian valleys of Paleozoic 
rocks below the Coal Measures, (Pennsylvanian) ; (3) the coal 
fields of the Pennsylvanian Series ; and (4) the Tennessee Val- 
ley, of the Mississippian Series, (Lower Carboniferous.) 

The Coastal Plain has two great basal systems, the Cretace- 
ous and Tertiary, and two blanket formations, the Grand Gulf 
and Lafayette. The Coastal Plain is' best adapted to general 
agriculture and is noted for its extensive forest growths. 

In both these great divisions of the State the topographic 
and other distinctive characters of the minor subdivisions are 
so intimately dependent on the geologic structure that it is de- 
sirable to discus's these features in connection with the geolo- 
gic formations. 

GEOLOGY. 

The subjoined table shows the chronological sequence of the 
geologic formations represented in Alabama, and the geologic 
map (PI. I.) shows their surface distribution. It may be added 
that the existence of certain late Tertiary marine formations 
in the lower counties of the State has been revealed by deep 
borings, while their outcrops have not as' yet been observed at 
the surface, a circumstance that is partly explained by the pres- 
ence in that section of two superficial formations, the Grand 
Gulf and the Lafayette, beneath which these marine deposits 
lie in places deeply buried. 



GEOLOGIC FORMATIONS OF ALABAMA. 



Quaternary* 



Tertiary. 



' Soils 
First bottom deposits and recent alluvium 
Second bottom deposits 
Columbia sands 
Lafayette 

Pliocene— S Grand Gulf 
| Pascagoula 

Miocene — Chattahoochee (Alum Bluff, Oak Grove, etc.) 

/ St. Stephens limestone 

Gosport greensand 
{ Lisbon beds 
Tallahatta buhrstone 



Eocene. / Chickasaw 

Or Wilcox 

j (Lignitic) 



Midway. 



Hatchetigbee 
Bashi (Wcods Bluff.) 
Tuscahoma (Bells Landing.) 
Nanafalia (Coal Bluff) 

Naheola (Matthews Landing.) 
Sucarnochee clay 



I Clayton limestone 



Cretaceous — -j 



f Ripley marl 

Selma chalk 

Eutaw sand 
I Tuscaloosa formation 



Carbcniferous. 



Pennsylvanian Series 
(Coal measures) 

f Bangor limestone 
Mississippiau Series ) j Oxmoor formation 
(Lower Carboniferous) \ } Tuscumbia limestone 

L Lauderdale chert 



Devonian — Chattanooga black shale 

Silurian — Red Mountain formation (Clinton) 

\ Pelham limestone (Trenton) 
/ Knox Dolomite 



Ordovician. 



Cambrian . 



C Coosa shale 
j Mcntevallo formation 
] Aldrich limestone 
[_ AVeisner sandstone 

/Talladega slates 



( Contempo- 
{ raneous. 
( Ft. Payne 
[ chert 



Metamorphic • 

and 
Igneous rocks 



'Ashland mica schists 
Igneous rocks 



\ Metamorphic Paleozoic strata; 
j Pennsylvanian in part 

| Metamorphic sediments of undetermined 
I age, probably Paleozoic 

{ Granites, diorites, gneisses, etc., of several 
{ages (pre-Cambrian and Paleozoic) 



6 physical geography, geology and climate, 

Appalachian Division. 

The main characteristics of the Appalachian area have al- 
ready been sketched. Its four subdivisions' will now be taken 
up more in detail, especially as regards the topography and ge- 
ologic structure, the discussion of the relation of these to the 
circulation of the underground waters being left to another 
chapter. 

Talladega Mountains and Ashland Plateau, (igneous and 
metamorphic rocks.) — These two sections' correspond with the 
Blue Ridge and the Piedmont plateau of Georgia and the 
States to the northeast. They make up the southeastern half 
of the Appalachian division, embracing part or all of Cleburne, 
Talladega, Clay, Coosa, Chilton, Elmore, Tallapoosa, Randolph, 
Chambers, Lee, and Macon counties. The rocks are all more 
or less crystalline in texture and fall into two general classes: 
(i)massive or dike rocks' of igneous origin, such as granite, 
diorite, and diabase; and (2) metamorphic or schistose rocks. 
The latter class is likewise divided into two divisions according 
to origin: (a) those derived from igneous rocks, such as the 
gneisses, the hornblende schists, the Hillabee green schists, etc., 
(b) and those derived from sediments, such as the feebly crys- 
talline phyllites of the Talladega Mountains, which are now 
known to be, at least in part, of the age of the Pennsylvanian 
series, (Coal Measures) ; the more fully crystalline mica-s'chists 
of the Ashland Plateau; and the quartzitey and crystalline 
marbles and dolomites. 

The planes of schistosity of these rocks, which may or may 
not coincide with original bedding planes, have in Alabama an 
almost universal dip to the southeast, giving a general north- 
east-southwest direction to all those topographic features which 
are due to the differential weathering of their outcropping 
edges. 

The Talladega Mountains, form the northwestern part of this 
subdivision. They are high, generally sharp-crested ridges 
with narrow, often gorgelike valleys between. These moun- 
tains, have an altitude of 2400 feet above sea level and are the 
highest peaks in the State. From this elevated land the country 
falls off rapidly on the west toward the great Coosa Valley, and 
on the east to the Ashland Plateau. The latter has an average 



GEOLOGY. / 

elevation above the sea of iooo feet. The plain-like character 
of this plateau is evidently the result of erosion — "base-leveling'' 
— and is not due to the horizontal position of the rocks', as is 
the case with the Cumberland Plateau, presently to be described. 
The surface of the Ashland Plateau is made up of beveled-off 
edges of the steeply dipping schists, and the present topo- 
graphic features are due to the subsequent elevation of this 
baseleveled plain and the dissection of its mass by the water- 
courses. 

The recent discovery of Carboniferous fossils on the eastern 
flank of the Talladega Mountain range where it merges into 
the Ashland Plateau, is evidence that some, at least, of these 
metamorphic rocks are of Paleozoic age. The southeastern 
half of the Plateau is in part made up of gneis'ses and mica- 
schists which are apparently older than the schists above men- 
tioned. This may be due, however, simply to a greater degree 
of alteration. Dikes of granite, diorite, gabbro, and other types 
of rock generally considered to be of unquestioned igneous 
origin are sometimes intruded between the schists', and fre- 
quently across them. 

In the western part of the Ashland Plateau these dikes in- 
tersect the Paleozoic schists and are, therefore, of Paleozoic or 
later age. In the eastern part, the dikes are intruded into schists' 
of possible pre-Cambrian age. A kind of metamorphosed trap 
rock or greenstone of peculiar character has been traced in an 
irregular line of outcrop from Chilton County, Alabama, into 
Georgia. This has been called the Plillabee Schist. It has been 
observed in Alabama only along the eastern base of the Talla- 
dega Mountain range, generally separating the slates of the 
Talladega Mountains from the mica-schists of the Ashland 
Plateau. 

Appalachian Valleys (Paleozoic formations below the Penn- 
syhanian). — The wide valley with prevailing calcareous soils 
lying between the Talladega Mountains on the east and Look- 
out Mountain and the Coos'a coal field on the west has received 
the name of Coosa Valley, from the river which drains it. It 
is the continuation and terminus of the Valley of East Tennes- 
see and the Great Valley of Virginia. Cahaba Valley lies be- 
tween the Coosa and Cahaba coal fields ; Wills Valley occupies 
the country between Lookout and Raccoon mountains. Both 



8 PHYSICAL GEOGRAPHY, GEOLOGY AND CLIMATE. 

of these valleys merge into the Coosa Valley between the end 
of Lookout Mountain and the Cahaba coal field. Between the 
Warrior and Cahaba coal fields are Shades and Jones' valleys, 
the latter at its north end branching into Coosa Valley on the 
one hand and Murphrees Valley on the other. Farther west, 
lying between Raccoon Mountain on the east and the Cumber- 
land Plateau on the west, is Browns or Blount Springs Valley, 
the prolongation in Alabama of the Sequatchee Valley of Ten- 
nessee. In structure all these valleys are anticlinal — that is, 
they have been eroded out of the crests of the long, narrow 
folds into which the strata have been bent by the compressing 
force acting from the southeast. With the exception of Mur- 
phrees Valley, these folds were lapped over toward the north- 
west and so have their steeper slopes on that side, while the 
gentle slope is toward the southeast. In Murphrees Valley the 
reverse is the case, the steeper slope being on the southeast side. 
The erosion to which these arches have been subjected has re- 
moved their crests, leaving only the remnants of the upbent 
strata to show by their position the original structure. 

In the Coosa Valley the structure is more complex. It is 
not a single anticlinal fold, but rather a series of folds, closely 
compressed, overlapping toward the northwest, and complicated 
by faulting and over-riding of the broken parts. Most of the 
present strata are the remnants of these folds'. They have in 
consequence a very general dip toward the southeast. In the 
other valleys the structure is more simple, since there is but a 
single arch, which is nearly always, broken or faulted on the 
northwest side, (on the southeast side in Murphrees Valley.) 

The steep dips above alluded to are always on the faulted 
side. By reason of the faulting, some of the strata are cut out 
and do not appear as they should in a normal anticline. 

The geologic formations occurring in these valley^ range 
from the lowest Cambrian up to the Pennsylvanian series, the 
latter, however, affecting the valley making only in the s'ense 
that it makes the summits of the bordering mountains. The 
most prominent of these formations is the Knox dolomite, a 
massive calcareous rock which generally occupies the central 
portions of the valleys. There are also other important lime- 
stones and calcareous shales, of Cambrian age, which form the 
floors of parts of these valleys, especially of the Coosa. All 
these limestones are interbedded with sandstones and chert. 



GEOLOGY. 9 

which stand out as subordinate ridges' that diversify all the val- 
leys. The Coosa Valley is thus a great trough, 30 miles wide, 
fluted with scores of parallel smaller valleys and ridges. The 
other valleys mentioned are of similar nature, but have less 
of these minor features'. 

The Weisner sandstone occurs, so far as the writer has ob- 
served, in the Coosa Valley region only. It is a veritable moun- 
tain-making formation, appearing most prominently in the 
range that extends from Alpine Mountain, near Coosa River, 
northeastward by Talladega, Oxford, and Anniston and on part 
Jacksonville into Georgia. The sandstones of the Red Moun- 
tain (Clinton) formation, as well as those of Mississippian se- 
ries (Lower Carboniferous,) in the southwestern part of the 
Coosa Valley, form a number of well-defined ridges. The sili- 
ceous or cherty parts' of two of the limestone formations — the 
Knox dolomite and the Lauderdale make prominent flint ridges 
in all the valleys ; the Lauderdale also caps the Red Mountain 
(Clinton) ridges of the smaller valleys. A great body of cal- 
careous shales and shaly limestones, appears in the "Flatwoods" 
of the Coosa Valley, extending from the Georgia line on both 
sides' of the river down to Gadsden and thence farther south- 
westward toward the north end of the Cahaba coal field. These 
are the Coosa and Montevallo shales of Cambrian age. 

The Pelham (Trenton) and Bangor limestones are of less 
importance in the valley making, though each is found in the 
subordinate troughs of the greater valleys. Shades Valley, 
which has been formed mainly out of the Bangor limestone, lies 
between Red Mountain, east of Birmingham, and Shades 
Mountain, the western escarpment of the Cahaba coal field, and 
forms a very important topographic feature of that section. 

These great valley regions are of extreme importance to Ala- 
bama from the fact that they contain the iron ores, bauxites, 
limestones, shales and clays, all of which have played a promi- 
nent part in the development of the State. 

Coal fields {P ennsylvanian scries.) — The coal fields are four 
in number — the Coosa, Cahaba, Lookout Mountain, and War- 
rior. They are separated from one another by long, narrow an- 
ticlinal valleys above described. Structurally they are troughs 
or synclines between these anticlines. In a general way it 
may be remarked that the synclinal troughs were much wider 



JO PHYSICAL GEOGRAPHY, GEOLOGY AND CLIMATE. 

than the anticlinal ridges; and that, away from the immediate 
vicinity of these uplifts, the strata of the coal fields are far less 
disturbed than are those of the adjacent valleys, retaining in 
general their original nearly horizontal position. By reference 
to the geological map it will be noticed that the expanse of near- 
ly horizontal strata of the coal becomes gradually wider and 
wider to the west and that the upward-bent wrinkles of the 
valleys are correspondingly narrower and farther apart. In the 
Coosa and Cahaba fields the syncline is unsymmetrical. Its 
axis lies close to its' Southeastern edge, in consequence of which 
the strata on the western side of the synclinal axis, embracing 
the greater part of the field, have a gentle southeasterly dip. 
On the eastern side they are sharply upturned, at times verti- 
cal, and give to these fields the appearance of being mono- 
clines. Cross' folds of minor character divide both these fields 
into several smaller basins. Lookout Mountain is a shallow 
synclinal trough well elevated above the valleys on each side 
of it. The same may be said of Raccoon Mountain, which forms 
the northern and northeastern parts of the Warrior field. 
Raccoon Mountain is capped by the Pennsylvanian rocks' and 
presents steep escarpments to the bordering valleys. That part 
of these fields in which the flat-topped summits of the highlands 
are capped with Pennsylvanian rocks, has been called the "pla- 
teau region." Across Tennessee River, in the northeast corner 
of the State, these plateaus are known as the spurs of the Cum- 
berlands. In the southwestern part of the Warrior field, how- 
ever, the strata of the Pennsylvanian series are found at levels 
ranging from that of the general drainage to far below it. This 
part of the field has been called the "basin region." It is' evi- 
dent that in the plateau region only the lower strata of the 
Pennsylvanian series are present, while in the basin region we 
may have, and in its routhwect end do have, the entire thickness 
of these rocks. The principal coal-mining districts are thus to 
be found in the western or southwestern parts of these fields, 
especially in the Warrior and Cahaba, and less conspicuously 
in the Coosa. The Lookout field is wholly in the plateau region. 

Valley of the Tennessee, (Mississippian series). — The area 
included under this head is naturally divisible into two parts', 
the first including the region east of Huntsville, bordered by 
the Cumberland mountains on the one side and Sand Mountain 



GEOLOGY. 11 

on the other. The second part embraces the valley west of 
Hnntsville to the Mississippi State line. 

From the northeast corner of the State down to- Guntersville, 
the river is confined to a long - narrow trough, known in Ten- 
nessee as the Sequatchee Valley, and in Alabama as Browns 
or Big Spring Valley. Below Guntersville the river flows in a 
northwest direction along a narrow, often gorge-like valley 
through the Cumberland Plateau to about the Meridian of 
Huntsville. It here emerges into the broad and open valley 
which is usually referred to as the Valley of the Tennessee. 

The geologic formations of this lower stretch of the river 
are the Bangor (Chester) limestone with its interstratified sand- 
stones', lying in general south of the river, while the country 
to the north is made by the siliceous limestones of the Tuscum- 
bia (St. Louis), the Lauderdale, and other members of the 
Mississippian series below the Bangor. These strata, while 
almost horizontal, have yet a perceptible dip to the south. The 
river crosses them nearly at a right angle to the dip, giving a 
Coastal Plain type of topography. The river itself occupies 
a broad trough in the Tuscumbia limestones, while on both sides 
are erosion ridges, with steep northward-facing slopes and gen- 
tle structural slopes on the south. North of the river these 
ridges are formed by the siliceous parts of the limestones. On 
the south the principal east-west ridge, known as Little Moun- 
tain, owes its existence to one of the intercalated sandstones in 
the Bangor limestone. Moulton Valley lies between Little 
Mountain and Raccoon Mountain. The Tennessee Valley, like 
the Coosa Valley, is a complex trough fluted with narrow par- 
allel ridges and subordinate valleys. Back from the river the 
red residual soils form some of the finest farming lands in the 
State. The cherty portions of the limestone from which these 
soils are derived remain as low rocky knolls which support a 
fine growth of oaks. The houses of the planters are usually 
located on these knolls. In the more broken part of the valley, 
between the immediate lowlands of the river and the northern 
boundary of the State, the large proportion of siliceous matter 
in the limestones makes' the soils in general inferior to those of 
the river plain. 



12 physical geography, geology and climate). 

Coastal Plain Division, 

The two fundamental systems of the Coastal Plain are the 
Cretaceous and Tertiary. They consist of interstratified beds 
of sand, clay, limestone, and marls, with their admixtures. 
These beds have an average dip toward the Mississippi embay- 
ment and the Gulf of Mexico, ranging from 30 to 40 feet to 
the mile. The surface of the Coastal Plain as a whole falls away 
in the same direction, but at a much less rapid rate — about 1 
foot to the mile — so that in going southward from the Appa- 
lachian area we pass in succession over the beveled edges of 
these formations from the oldest to the newest. Each of these 
formations, with the exception of some of the Miocene and 
Pliocene, occupies the surface in a belt proportional in width to 
its thickness and running approximately east and west across 
the State. 

After the close of Tertiary time there was deposited a blanket 
formation which is of great importance in the Coastal Plain. 
It is known as the Lafayette formation, and is a mantle of red- 
dish and light-colored loams and sands, with frequent beds of 
waterworn pebbles in the lower parts. It has an average thick- 
ness of 25 to 30 feet and formerly covered the entire area of 
the Coastal Plain. It rests! unconformably on the older for- 
mations following the topography in general very closely, 
though in many large areas it has been in great part removed 
by erosion. As a consequence this formation makes perhaps 
four-fifths of the cultivated soils of the whole plain, and its sig- 
nificance in relation to the underground waters, which appear 
in springs and shallow wells, cannot well be overestimated. 

The characteristics of the several divisions of the Creta- 
ceous, Tertiary, and Quaternary systems will here be reviewed 
in a general way, many details being left for consideration in 
connection with their relations to the underground water supply. 

The combined thickness of the Cretaceous formations in 
Alabama has been estimated to be about 2500 feet; that of the 
Tertiary formations classed as Eocene in the table, about 1800 
feet. The thickness of the post-Eocene strata can not yet be 
stated with much certainty, though in some deep borings at 
Mobile, Miocene shells found at a depth of over 1500 feet. 



GEOLOGY. 13 

CRETACEOUS. 

The Cretaceous system in Alabama includes four formations 
which arc, in ascending- order : 

( i ) The Tuscaloosa, a formation of freshwater origin, 
made up in the main of sands and clays in many alternations. 

(2) The Butaw, a formation of marine origin, composed of 
s'ands and clays more or less calcareous, but nowhere showing- 
beds of hard limestone. 

(3) The Selma Chalk, likewise of marine origin, a great 
calcareous formation of the nature of chalk, with varying ad- 
mixtures of clay and other impurities'. 

(4) The Ripley, also a marine formation in which the cal- 
careous constituents generally predominate, but in parts con- 
taining sandy or clayey beds. 

None of these formations greatly affects the topography or 
has marked lithologic characters except the Selma chalk. This 
underlies a belt entering the State from Mississippi and ex- 
tending eastward with an average width of 20 to 25 miles', to a 
short distance beyond Montgomery, where its distinctive char- 
acters are lost or merged into those of the "blue-marl region," 
to be more particularly treated later. The somewhat uniform 
composition of the Selma chalk has caused it to be more deeply 
and evenly wasted by erosion and solution than the more sandy 
formations north and south of it. As a consequence, its' out- 
crop is in the shape of a trough, with a gently undulating, al- 
most unbroken surface except where remnants of the once con- 
tinuous Lafayette mantle have protected the underlying lime- 
stone from erosion and have thus formed knobs and ridges 
capped with its loams and pebbles. 

In this belt, more than in any other of the Coastal Plain, the 
s'oils show their residuary character. They are, as a' rule, 
highly calcareous clays and, where much mixed with organic 
matters, of black color. Throughout this section are areas orig- 
inally destitute of trees and hence known as "prairies". From 
the agricultural point of view, the Selma chalk or black belt is 
the most highly favored part of the State and, apart from the 
cities, holds the densest population. 



14 PHYSICAL GEOGRAPHY,, GEOLOGY AND CLIMATE. 

The Eutaw and Tuscaloosa formations outcropping north of 
the prairie or Selma chalk belt, show no marked topographic 
features'. The relatively broken and uneven topography of the 
Tuscaloosa area results largely from the preponderance of 
loose or slightly indurated sands with subordinate beds of plastic 
clay in the formation. The general absence of lime and phos- 
phate from the strata causes comparatively poor soils. The 
most important features of some parts of this territory are, or 
rather were, the grand forests of long-leaf pine, now practically 
exhausted. The surface of the Eutaw belt is generally smoother 
than that of the Tuscaloosa, and the calcareous character of 
many of the sandy and clayey beds insures greater fertility. 

The Ripley formation, south of the Selma area, has many 
features in common with the Eutaw, and while prevalently 
sandy, it yet contains a very considerable proportion of lime- 
stone and calcareous clays. 

As has been intimated above, the Selma chalk seems to give 
out a short distance east of Montgomery, and the whole ma- 
rine Cretaceous section takes on a very uniform lithologic char- 
acter, being composed in the main of a bluish sandy marl in 
which scales and flakes' of mica are numerous. The lower beds 
of the blue marl might perhaps be discriminated from the rest 
by the presence of certain fossils of the Eutaw horizon. In the 
eastern part of the State, however, the three marine Creta- 
ceous formations, so clearly distinct in the western part, are 
represented by a series of beds of rather uniform lithologic 
character, though perhaps sufficiently distinct in their fossils. 

TERTIARY. 

Eocene. 

In the western half of the State, in the vicinity of Alabama 
and Tombigbee rivers, the succession and thickness of the 
strata from the base of the Tertiary up to the top of the St. 
Stephens limestone, have been ascertained with a considerable 
degree of accuracy. Eastward to the Chattahoochee, less work 
has been done, but the formations have been fairly well studied 
and their succession and thickness along the Chattahoochee are 
also very well established, chiefly by the work of Mr. D. W. 
Langdon. These strata, which are usually classed as Eocene, 
have a thickness of about 1800 feet and present the following 
characteristics : 



GEOLOGY. 15 

MIDWAY GROUP. 

Clayton limestone. — At the base of the Tertiary' is found an 
impure limestone, thin and inconspicuous in western Alabama, 
but thickening to the east until on Chattahoochee River it in- 
cludes fully 200 feet of alternating calcareous sands and lime- 
stones. This formation is called the Clayton limestone. 

Sucarnochee clay. — Next above the Clayton there is, along 
Tombigbee River, a series of black or dark-brown clays at 
least 100 feet thick. This formation is als'o well exposed at 
Black Bluff on Tombigbee, and on Sucarnochee River, and 
has been called Sucarnochee. At Black Bluff and sparingly at 
a few other points these clays are fo^siliferous. While nearly 
devoid of lime in the Tombigbee drainage, except in the lower- 
most strata, the clays become more and more calcareous to the 
east, and in Wilcox county, east of Alabama River, they form 
the basis of some fine black prairie lands'. The formation east 
of Wilcox County has not been traced. 

Xaheola formation (Matthews Landing.) — Next above the 
Sucarnochee clays is the Naheola formation, embracing 150 
feet or more of gray sandy clays, with some beds of dark sandy 
glauconitic clay contaaining marine fossils near the base. To 
the east this formation appears to die out and it is not found ex- 
posed on Chattahoochee River. 

CHICKASAW ( WILCOX ) GROUP. 

Between the top of the Sucarnochee clay and the base of the 
Tallahatta buhrstone lies a group which Dr. Hilgard, in his re- 
port on the Geology of Mississippi, called the Lignitic. 

The term LaGrange was used by Dr. Safford of Tennessee, 
to include a portion of the beds originally termed Lignitic by 
Hilgard. LaGrange is a locality name and would doubtless 
have stood but for the fact that Safford included in it the La- 
fayette (Orange Sand), and a portion of the Cretaceous. The 
name Lignitic being also deemed inadmissible, because descrip- 
tive, the term Chickasaw, from the Chickasaw Bluffs near Mem- 
phis, was proposed by Dr. Hilgard and Prof. Dall as a substi- 
tute, to include the beds grouped by Hilgard under the term 
Lignitic, excluding what he termed the Flatwoods belt. In this 



16 PHYSICAL GEOGRAPHY, GEOLOGY AND CLIMATE. 

sense the name was duly accepted by the geologists and has been 
used by Prof. Dall and others since 1895. Some objection 
seems to have arisen to this name also, and in a recently pub- 
lished report, by Messrs. Eckel, Crider and Johnson, on the 
Underground Water Resources of Mississippi* the term Wil- 
cox, from Wilcox County, Alabama, where these beds are 
characteristically developed, is substituted for Chickasaw, and 
embraces the Nanafalia, the Tuscahoma, the Bashi, and the 
Hatchetigbee formations. In the present Report the accepted 
term Chickasaw is retained for this group with the alternative 
of Wilcox in case the objection to the former name proves to 
be well founded. 

This is the most massive of these divisions, having a thick- 
nes's which is probably not less than 900 feet. It also presents 
a great variety in lithologic character and in fossil contents. 
In the most general terms the Chickasaw or Wilcox strata are 
cross-bedded sands, thin-bedded or laminated sands, laminated 
clays, and clayey s'ands, with beds of lignite and lignitic matter 
which merely colors the sands and clays'. With these are found 
interbedded at several horizons strata containing marine and 
estuarine fossils. The fossil-bearing beds 1 ' form the basis for 
the separation of this group into four formations, given in 
some detail below. 

Nanafalia formation (Coal Bluff.) — The Nanafalia overlies 
the Naheola, and maintains a tolerably uniform thickness of 
about 200 feet entirely across the State. These beds are mostly 
sandy, but contain great numbers of the shells' of a small oys- 
ter, Gryphoea thirsae. Near Alabama River and for a short 
distance to the east, a gray siliceous clay with a tendency to 
indurate into a tolerably firm rock resembling very closely some 
of the strata of the Tallahatta buhrstone of the Claiborne group, 
presently to be described, is a characteristic feature of the whole 
section. At the base of the oyster-shell beds there are, at cer- 
tain localities, other fossiliferous beds containing a great va- 
riety of forms. 

At the bottom of the Nanafalia formation there is a bed of 
lignite, 5 to 7 feet thick, which may be traced across the country 
from Tombigbee River into Pike County, where it is well ex- 
posed near Glenwood station, not far from Troy. 

*Water Supply Paper, No. 159, U. S. Geological Survey. 



GEOLOGY. 17 

The Nanafalia sands will be considered again in another 
chapter in connection with the underground water supply of 
some parts of the State. • 

Tuscahoma formation (Bells Landing.) — These beds are 
about T40 feet thick and consist mainly of gray and yellow 
cross-bedded sands and sandy clays, generally poor in fossils 
except at one horizon, which is typically exposed at the locali- 
ties from which the two names above have been taken. 

Baslii formation (Woods Bluff). — Above the Tuscahoma is 
the Bashi which averages perhaps 80 feet in thickness. It is 
composed of the sands and sandy clays common in the Tertiary. 
It is distinguished by a characteristic bed of highly fossiliferous 
greensand with associated beds of lignite immediately below it. 
By these features the Bashi may be easily identified across the 
width of the State. — -The best exposure of the fossiliferous 
green sands of this formation is at Woods Bluff on Tombigbee 
river. 

Hatchetigbee formation. — The uppermost formation of the 
Wilcox group is composed of beds of brown, purple, and gray 
laminated sandy clays and cross-bedded sands abounding in 
characteristic fossils. It is about 175 feet thick in the vicinity 
of Tombigbee River, but it thins to the east, though otherwise 
maintaining its distinctive character. These beds have been 
named Hatchetigbee, from a bluff on Tombigbee River. They 
will be referred to again in the discussion of the underground 
waters. 

CLAIBORNE GROUP. 

Between the Chickasaw group and the base of the St. Steph- 
ens limestone lie the strata of the Claiborne group easily divi- 
sible in Alabama, into three formations', the lower being the 
Tallahatta Buhrstone, the middle being the Lisbon formation 
and the upper, the Gosport Greensand. 

Tallahatta buhrstone. — In the western part of the State the 
most prominent rocks of this formation are aluminous sand- 
stones or siliceous claystones. They vary slightly in composi- 
tion, but are always' poor in fossils except the microscopic sili- 

2 



18 PHYSICAL GEOGRAPHY, GEOLOGY AND CLIMATE;, ' 

ceous shells of marine diatoms and radiolaria. To the east 
the percentage of clay decreases, the rocks become more cal- 
careous, and the fossils are more abundant, and in place of the 
silicified shell casts of the Tombigbee and Alabama drainage 
basins are extensive beds of shells, mostly oyster shells. The 
thickness of the buhrstone varies from 400 feet in the western 
part of the State to 200 feet in the eastern part. In the wes- 
tern part of Alabama and still more in Mississippi, beds of fos- 
siliferous! green sand are abundant in both the Tallahatta and 
in the Lisbon strata of the Claiborne. The decay of the green- 
sands has in many places given rise to the accumulation of de- 
posits of brown iron ore which may some day have a commer- 
cial value. The Tallahatta Buhrstone as here defined is the 
equivalent of the Siliceous Claiborne of Hilgard. 

The Lisbon Formation. — Between the Buhrstone and the base 
of the Gosport greensand are' the Lisbon beds consisting of 
about 115 feet of calcareous clayey sands and sandy clays gen- 
erally fossiliferous. 

The lower half of these beds' contains a great number and va- 
riety of well preserved shells; in the upper half the shells of 
ostrea sellaeformis and several species of pecten greatly pre- 
ponderate over other forms. The most characteristic exposures 
in Alabama of these beds, which are the equivalents of Hilgard's 
Calcareous Claiborne, are at the Claiborne and Lisbon Bluffs 
on the Alabama river. 

The Gosport Greensand. — This division, which, so far as' yet 
known, does not appear in any other of the Gulf States,' 
embraces the strata of the Claiborne group lying between the 
top of the Lisbon, and the base of the St. Stephens. The beds 
are in general highly glauconitic sands about thirty feet in 
thickness at the Claiborne and Gosport bluffs and include the 
fossiliferous greensands which have made the name Claiborne 
famous, and which have furnished the greater part of the 
Claiborne fossils described and figured by Conrad and Lea. 
While this division, as above mentioned, is not known in Miss- 
issippi, Louisiana or Texas, yet its importance in Alabama, from 
the historical point of view and because of the great number and 
variety and beautiful state of preservation of its fossils, is 
such as to compel mention and a distinct name. This member 



GEOLOGY. 19 

of the Claiborne group has been observed at a number of local- 
ities in Monroe, Clarke, Choctaw and Washington counties. 
The name is from Gosport a landing on the Alabama river a 
few miles below the Claiborne Bluff. 

St. Stephens limestone. — Above the Claiborne, and constitu- 
ting the uppermost member of the Eocene in Alabama, is the 
St. Stephens limestone, equivalent in part to the Vicksburg lime- 
stone and in part to the Jackson limestone of Mississippi. In 
Alabama these two formations blend so completely that it has 
been impossible to draw clearly the line of demarkation between 
them, and the St. Stephens is therefore intended to include the 
Alabama representatives of both. Immediately overlying the 
Claiborne fossiliferous sands, at many points in Clarke, Choc- 
taw, and Washington counties, is an argillaceous limestone 
closely resembling the Selma chalk and like it giving rise to 
rich black limy soils. The fossils of this bed show that it is 
probably of Jackson age, but the great mass of the St. Stephens 
formation, between 200 and 300 feet thick, consists of a lime- 
stone of a considerable degree of purity in which the ever pres- 
ent fossil is a nummulitic shell, Orbitoid.es iyelli. Other shells 
also abound, but this is characteristic. This limestone shows 
many variations, being in some cases hard, almost crystalline, 
capable of a high polish, of a pleasing variety of color, and 
hence probably well adapted for ornamental construction. Com- 
monly, however, the rock is soft and easily cut with a saw, axe, 
or plane when fresh from the quarry, and it is much used in the 
construction of chimneys and pillars to houses. On this ac- 
count it is well known from Texas to Florida as the "chimney 
rock." In the southeastern part of the State and in Georgia 
this limestone has frequently become silicified, and great masses 
of it appear to have all of the lime replaced by silica. The 
bones, particularly the vertebrae, of an extinct whale, Zeuglo- 
don, are in some localities abundant in the lower (Jackson) di- 
vision. 

Topographic features of the Eocene.- — In general it may be 
said that the part of the State in which the Eocene strata occur 
is a gently sloping plain into which the streams have sunk their 
valleys, leaving between them remnants of the original mass as 
hills. Two or three formations of the groups impress them- 



20 PHYSICAL GEOGRAPHY, GEOLOGY AND CLIMATE. 

selves on the soils and the topography more forcibly than the 
others. The first of these is the great bed of black clays of the 
Sucarnochee horizon, underlying a belt of country known west 
of Alabama River as the "Flatwoods" or "Post Oaks." East 
of this river these clays are strongly calcareous and give rise 
to black prairie soils. The Flatwoods proper constitute a sort 
of trough 5 or 6 miles wide, badly drained and little cultivated, 
with a heavy growth of small post-oaks and short-leaf pine. 
During wet weather the Flatwoods have all the characteristics, 
of a swamp. Along the northern border of this belt the clays 
are often highly calcareous, and the transition from the limy 
Cretaceous formations to the tough plastic clays of the genuine 
Flatwoods is very gradual. 

The next member of topographic importance is the Nanafalia 
especially in that part of the State west of the drainage area 
of Alabama River. In this section there is a considerable thick- 
.ness of indurated clayey sands — sandstones, in fact — overlying 
the oyster-shell bed. This gives rise to a very broken and hilly 
country, as shown in the Grampian Hills of Wilcox County. In 
the eastern part of the State there are many "sinks'" and big 
springs in the Nanafalia territory. 

Farther south the outcrop of the Tallahatta buhrstone, es- 
pecially in the western half of the State, makes veritable moun- 
tains, often rising with steep northwardfacing slopes 200 feet 
or more above the adjacent lowlands. In Clarke and Choctaw 
counties, and in still greater degree in Mississippi, these buhr- 
stone mountains, with their rocky slopes, remind one of the Ap- 
palachian region. 

In the eastern counties the Clayton limestone acquires ex- 
ceptional thickness, 200 feet or more, and shows the character- 
istics of limestone terranes' such as caves, lime sinks, and "big 
springs." The St. Stephens limestone also gives rise to broken 
country with characteristic caves and other features. Along 
the northern edge of this (St. Stephens) outcrop the strong, 
limy, black soils formed by the clayey limestone resemble the 
black prairie soils of the Selma chalk, but the topography of 
the country offers strong contrast — in the chalk, softly undula- 
ting, almost level lands ; in the lower St. Stephens, exceedingly 
broken and deeply eroded lands, justifying the name "lime 
hills." 



GEOLOGY. 2 L 

As has been indicated above, the trunk streams of the Ala- 
bama Coastal Plain How across the outcropping strata, while 
their tributaries flow in general parallel to the strike of these 
outcrops. In the gradual sinking of the beds of these tributary 
streams the characteristic Coastal Plain topography is devel- 
oped ; the in facing slopes of the hills are precipitous, while the 
gulfward slopes are gentle. The streams have their place gen- 
erally at the base of the steep infacing slopes. 

Miocene, 
chattahoochee series. 

In 1889 Mr. D. W. Langdon of the Alabama. Geological Sur- 
vey, discovered on Chattahoochee River a new series of marine 
calcareous formations of Miocene age, overlying the Vicksburg 
limestone. This series he called the Chattahoochee from the 
town and landing of that name. 

With the exception of some sandy clays on Conecuh River, 
which hold a few poorly preserved fossils of the Chattahoochee 
horizon, none of these beds has up to the present time been 
found to outcrop in Alabama, for the reason that the section 
of the state in which these outcrops would normally occur is 
covered with a thick mantle of two superficial formations, the 
Grand Gulf and the Lafayette. In addition to this that portion 
of the region contiguous to Mobile river in which we should 
expect to find the outcrops, is of the nature of a delta with low 
alluvial banks. It is safe, however, to say that these Chatta- 
hoochee formations' underlie the southern part of the State be- 
neath the superficial deposits mentioned, for deep borings in 
Mobile and Baldwin counties have demonstrated their existence 
at depths between 800 and 1550 feet, by means of the shells 
characteristic of the several horizons brought up by the drills. 

Pliocene, 
pascagoula. 

In 1889, Mr. L. C. Johnson, also of the Alabama Survey, dis- 
covered on Chickasawhay river in Mississippi a few miles above 
its confluence with Leaf river to form the Pascagoula, a highly 
fossiliferous marine or estuary deposit to which he gave the 



22 PHYSICAL GEOGRAPHY, GEOLOGY AND CLIMATE. 

name Pascagoula. This bed has as yet been seen in outcrop 
only at the type locality and, according to Mr. Dall, at Shell 
Bluff on the Pascagoula river*. At the type locality it under- 
lies strata of the Grand 'Gulf formation. Most of the shells of 
this bed are of a new species, (Rangia Johnsoni) ; but along 
with these are numerous shells of Ostrea Virginica, by Mr. 
Dall's determination. As this latter species is not known to 
occur in strata older than Pliocene; the Pascagoula is placed in 
this formation in our classification. 

In the artesian wells at Mobile shells' characteristic of the Pas- 
cagoula horizon are brought up from depths of about 700 feet. 
We may therefore be reasonably certain that this formation, 
like the Chattahoochee, underlies the lower part of the State 
though its outcrop for reasons given, has not yet been discov- 
ered. 

GRAND GULF FORMATION. 

This name was given in Mississippi to a series of sands and 
clays of varying character and varying degree of induration, 
overlying directly and unconformably the Vicksburg limestone, 
and, together with the next overlying Lafayette beds, forming 
the surface of the Coastal Plain of that state down to within ten 
miles of the Gulf of Mexico. More specifically the strata are 
thin-bedded and massive clays of colors varying from white 
through shades of red and brown to black, interstratified with 
sands', the latter in many places indurated to form sandstones, 
with aluminous or siliceous cement. Occasionally these rocks 1 are 
even quartzitic, as at the' type locality and in a number of places 
in Georgia and Alabama, but as a rule they are only slightly 
coherent. The clays also in part are indurated into mudstones, 
and in part are more or less plastic. The presence of lignitic 
matters and of gypsum is also locally characteristic of the clays, 
many of which are quite meager because of intermixture with 
fine grained sand. In Alabama the prevailing materials are 
massive clays' of reddish to brown colors .or mottled gray to red 
and laminated clays interbedded with sands varying in coher- 
ence from loose sands to firm sandstones and aluminous or 
siliceous cement. The aluminous sandstones pass by insensible 

*This may be the same as the type locality, which is also called 
Shell Bluff. E. A. S. 



GEOLOGY. 23 

gradations into meager clays which are themselves often indu- 
rated into mudstones as compact as some of the sandstones. 

While the induration of the sands is common in Mississippi 
along the border of the river valley from Grand Gulf down to 
the Louisiana line, and thence eastward beyond Brandon, it is 
by no means confined to those bounds as some are disposed to 
believe. In Georgia in all parts of the Altamaha Grit region, 
occasional occurrences of the exceedingly hard, sometimes 
quartzitic, sandstones are known down to within a few miles 
of the Atlantic coast. It may be here remarked that the exces- 
sive siUcification, often resulting in the complete obliteration of 
the original texture of the rock, as is the case in one of the 
sandstone ledges at the type Grand Gulf locality, is by no means 
confined to that locality nor, indeed to the rocks of the Grand 
Gulf formation, for in the southeastern parts of Alabama and 
southwestern of Georgia adjacent, much of the Vicksburg 
limestone has been so completely petrified by silica that not a 
trace of lime remains, and many of the masses of Miocene co- 
rals so common in Southwestern Georgia are completely silici- 
fied, being interiorly a mass of amorphous silica devoid of all 
trace of organic structure. These remarks are made in con- 
nection with a proposition to restrict the name Grand Gulf to 
the quartzitic sandstone occurring at the type locality. 

While the inner or landward border of the Grand Gulf man- 
tle is in contact with the Vicksburg limestone in Mississippi and 
with the St. Stephens in western Alabama, from Govington 
county in the latter state eastward it is found lapping succes- 
sively over the older Tertiary formations, and about Clayton 
and Eufaula and in adjacent parts of Georgia, even over the 
Ripley beds of the Cretaceous. On the map accompanying this" 
report only this landward margin of the formation is attempted 
to be shown. Below or southward of this line its strata cover 
partially the outcrops of the upper Cretaceous and older Ter- 
tiary beds, while those of the newer Tertiary, Chattahoochee 
and Pascagoula, with the exception of the exposure on the 
Conecuh river above mentioned, seem to be completely hidden 
by it and the closely associated Lafayette. Along the Chatta- 
hoochee river south of the Alabama line, however, the whole 
series of these newer Tertiary beds (possibly excepting the 
Pascagoula,) is clearly exposed, with the Grand Gulf and La- 
fayette beds overlying them. In Alabama as yet we have onlv 



24 PHYSICAL GEOGRAPHY, GEOLOGY AND CLIMATE. 

the evidence afforded by the deep borings in Mobile and Bald- 
win counties, to prove that below the surface occupied by the 
Grand Gulf and Lafayette beds, all the Miocene and Pliocene 
marine Tertiary formations above mentioned are reached at 
depths between 200 and 1550 feet. All the facts derived from 
observations in Mississippi, Alabama, Georgia, and Florida 
seem to show that the Grand Gulf formation cannot be older 
than upper Pliocene, since it overlies often by an interval cf 
many feet, the Pascagcula shell bed with Ostrea Virginica. 
In these states no formation older than the Lafayette is known 
to overlie it. 

It is impossible to give with certainty the thickness of the 
Grand Gulf strata. The dip in some parts of its territory seems 
to be no greater than the general slope of the land surface ; ui 
this' respect it resembles the Lafayette. In Mobile and Baldwin 
counties the thickness above sea-level is at least 150 feet, and 
in the borings mentioned a greater but undetermined thickness 
is found. The absence of fossils, except plant remains and a 
. few fresh water unios, makes the fixing of the exact age of the 
formation difficult ; in this also it resembles the Lafayette. 

In the lower counties of the State the Grand Gulf is one of 
the most important formations in relation to underground wa- 
ters, and more detailed mention of it will be made later. 

QUATERNARY. 

LAFAYETTE FORMATION. 

The surface distribution of this great mantle formation, or 
rather its landward limit, will be seen by" the map. In general 
it consists of a red sandy loam, usually devoid of stratification 
in the upper part, with cross-bedded sands and irregular beds of 
water-worn pebbles in the lower part. 

The thickness does not often exceed 25 feet, and it follows 
the contours of the surface very closely, being a veritable blan- 
ket; sometimes completely washed away, but varying very 
little in thickness whether on the high level interstream plateaus 
or along the slopes which break away from them. 
It overlies with uncomfortable contact every formation in Ala- 
bama from the oldest up to the Grand Gulf inclusive. 



CLIMATIC. 25 

Since all the high table lands, remnants of the p'ain into 
which the streams have worn their valleys, arc covered by the 
red loam of this formation its importance as a soil former is 
obvious. In yet another particular its importance cannot be 
overestimated, namely, in its relations to the underground wa- 
ters. Its loam and pebble beds are storage reservoirs' of count- 
less springs and shallow wells over the entire Coastal Plain. 
Other detai's will be given in connection with the discussion of 
the underground water distribution. 

LATER FORMATIONS. 

The later formations, Columbia, Second Bottom deposits, 
First Bottom and other recent alluvial deposits, and soils, may 
be here passed over with mere mention, and with the remark 
that no sure identification of the Columbia has been made in 
Alabama, though some gray and white sands frequently seen 
overlying the Lafayette are probably of this age. 



CLIMATE OF ALABAMA. 

BY MR. FRANK P. CHAFFEE, 

Section Director, U. S. Weather Bureau, Montgomery, Ala. 
(By permission from an article prepared for the Climatolog- 
ical Department of Agriculture.) 

General Features. 

In the preparation of this climatic summary, reference has 
been made to the reports of the Smithsonian Institution and of 
the United States Signal Service, now the Weather Bureau ; to 
Bulletin No. 18 of the Agricultural Experiment Station at Au- 
burn, Ala. ; and to the reports of the various voluntary observers 
in Alabama co-operating with the Weather Bureau. 

In its distance from the equator, elevation above sea level, 
configuration of its mountain chains, proximity to the sea, and 
prevailing winds, Alabama is favorably situated for a temper- 
ate and comparatively uniform climate. In the extreme south- 
western portion, washed by the water of the Gulf of Mexico, 
the climate approaches the subtropical, while the climate in the 
highlands of the northeast is similar to that of regions' of less 



26 PHYSICAL GEOGRAPHY, GEOLOGY AND CLIMATE. 

elevation much farther north. Extremes of temperature are 
rare. Over the southern half of the States the heat of the sum- 
mer is tempered by the prevailing- winds from the Gulf, and ; n 
the more northern counties the elevation secures immunity 
from excessively high temperature. Freezing temperatures do 
not often continue longer than 24 to 48 hours. Snow rarely 
falls, except in the northern counties, where it occurs on an av- 
erage of about twice each winter and seldom remains on the 
ground for more than 48 hours. The rivers do not freeze. 
With the exception of the country along the Gulf Coast, whert 
the precipitation is heavy, the rainfall is well distributed. The 
growing season is so long that often two and sometimes three 
minor crops are raised on the same ground in one year. 

Temperature. 

The average temperature of the entire State is 63 degrees; 
for the southern portion, 66 degrees'; middle portion, 64 de- 
crees ; northern portion, 60 degrees. Highest average, 67 de- 
grees, in Baldwin and Mobile counties ; lowest average, 60 de- 
grees 1 , in Dekalb County. The average by seasons is as follows : 
Winter, 46 degrees ; spring, 63 degrees ; summer, 79 degrees ; 
autumn, 63 degrees. The average summer maximum is 90 de- 
grees and the average winter minimum 35 degrees. The abso- 
lute maximum, 109 degrees, occurred at Lock No. 4 (Lincoln), 
Talladega County, July 7, 1902 ; the absolute minimum, 17 de- 
grees below zero at Valley Head, Dekalb County, February 
13, 1899. Average number of days per year with temperature 
above 90 degrees, 62 ; average number of days per year with 
temperature below 32 degrees, 35. The temperature seldom 
falls below zero, the above extremely low reading being re- 
corded during the severe cold wave of February 12-13, 1899, 
which gave the coldest weather ever recorded or remembered 
in this section.* 

Killing Frost. — The average dates of last killing frost in 
spring are as follows : northern district, April 6th ; middle, 
district, March 23rd ; southern district, March 9th ; for the state, 
March 2rd. Average dates of first killing frost in autumn : 

*Since preparing this article a temperature of 18° below zero oc- 
curred at Valley Head, Dekalb County, February 14, 1905. P. P. C. 



CLIMATE. 27 

northern district, October 20th; middle district, November 5th; 
southern district, November 17th; for the state, November 4th. 
This gives' average growing seasons as follows ; northern dis- 
trict, 197 days; middle district, 227 days; southern district, 
253 days ; for the state, 226 days. The latest killing frost 
known, May 2nd, 1897, a * Oneonta, Blount Co. ; with this ex- 
ception, the latest on record, was April 30th, at Valley Head, 
Dekalb County. The earliest killing frost of which there is 
official record was October 2nd, at Decatur, Morgan County, 
but the voluntary observer at Oneonta reports' that there is a 
record of killing frost having occurred at that place, September 
4th, 1866. Over the middle counties, the last killing frost, as a 
rule, occurs during the first half of April, and where the last 
frost is recorded in March, the records show its formation dur- 
ing the early part of April was prevented by cloudy weather 
or fresh to brisk winds. The first killing frost usually occurs 
over the middle counties during the last half of October. When 
the first frost occurred in November, the records show that at 
the same time during the last half of October the temperature 
was low enough for frost, the formation of which was prevent- 
ed by conditions mentioned above. 

The distribution of the temperature is shown by the subjoined 
chart. 



28 PHYSICAL GEOGRAPHY, GEOLOGY AN'D CLIMATE. 




Fig. 1. — Map showing 



mean annual temperatures (Fahrenheit) in 
Alabama. 



Precipitation. 



Annual precipitation for the State as a whole, 52 inches ; 
for northern district, 52 inches; middle district, 51 inches; 
southern district, 55 inches. The distribution of precipitation 
is shown by the accompanying chart. The greatest annual av- 
erage — from 62 to 63 inches' — is in the southwestern counties, 
bordering on the Gulf of Mexico. Another region of heavy 
precipitation is found over the mountainous (north-central and 
north-eastern) portions, where it ranges from 47 to 54 inches 
per annum. The region of least precipitation is near the center 
of the State, where the annual average is about 46 inches. The 
precipitation is practically all rain. Snow occurs on an average 
twice each winter in the northern half of the State and about 



CLIMATE. 29 

once a winter in the southern counties ; it varies from very light 
in the southern district to moderately heavy (about 8 to 14 
inches) in the north-central and northern counties', ft is not 
common for a winter to pass without snow enough to cover 
the ground. in any portion of the State. The precipitation is 
well distributed throughout the growing season, especially in 
the middle and most important agricultural counties, and the 
autumns are, as a rule, favorable for the maturing and gather- 
ing of the staple crops. 

Fog. — Dense fog seldom occurs, and then generally in the 
winter or spring months, and is mostly confined to the coast 
district. 

Hail. — This occurs occasionally during the spring and sum- 
mer months, though really destructive hailstorms are rare in 
this section. 

Thunderstorms. — These occur in some portions of the State 
during every month of the year, being most frequent during 
the summer months. The most severe thunderstorms occur 
along the Gulf coast, and in the west-central counties. 



30 



PHYSICAL GEOGRAPHY, GEOLOGY AND CLIMATE. 




Fif 



2.- — Map showing average annual precipitation in inches for 
Alabama. 



Winds. 



The prevailing direction for the year is south ; for winter, 
north ; spring, south ; for summer, south ; for autumn, north. 
Average hourly velocity, (computed from records at Mobile 
and Montgomery only), 7 miles. The highest velocity ever 
recorded, was 72 miles from southeast at Mobile October 2nd, 
1893. Winds' of 40 miles per hour or more have occurred as 
follows: Mobile (record from 1885 to 1893 inclusive) 23 
times, or on an average or a little more than once a year. Mont- 
gomery, (record from 1875 to 1903 inclusive), 12 times, or 
an average of about once in three years. 

During the passage of general storms over and to the north 
of this region, destructive wind storms or tornadoes have oc- 



PHYSICAL GEOGRAPHY, GliOLOGY AND CLIMATIC. 31 

curred as follows : Year of greatest frequency, 1884, with 19 
storms; average yearly frequency 1.6 storms; year in past twen- 
ty-three with no report of storms, none; month of greatest fre- 
quency, March; day of greatest frequency, January nth; 
hours of greatest frequency, 6 to 8 p. m. ; months' without such 
storms, July, August, September, and October; prevailing di- 
rection of storm movement,, southwest to northeast; region of 
greatest frequency, north central portion. 



CHAPTER 11. 

A. GENERAL DISCUSSION OF UNDERGROUND 
WATERS. 

SOURCE OF CIRCULATING WATERS. 

The ocean, which covers three-fourths of the surface of the 
earth is' the chief source from which is derived the water which 
circulates through the atmosphere, and upon and through the 
lands, and the great reservoir into which most of these waters 
finally return.* 

By evaporation from its surface, moisture is taken up into 
the atmosphere to be condmsed and to fall as rain or snow e ther 
directly back into the ocean, or upon the land surface and from 
it back into the universal reservoir by several ways more par- 
ticularly to be mentioned below. In this' passage, the water may 
be temporarily locked up and withdrawn from circulation in the 
tissues of organic beings, animal and vegetable, and in minerals, 
but eventually practically all joins again the great cycle. 

As has been shown in a previous chapter, the amount of this 
rainfall for the state of Alabama, averages about 52 inches per 
annum. 

DISPOSITION OF THE WATER FALLING UPON THE LAND 

SURFACE. 

The water falling upon the surface of the land is disposed of 
in the following ways: (1) A part is restored directly to the 
atmosphere by evaporation from the surface without previous 
absorption, (2) a part runs directly into the streams without 
being first absorbed by the soil, and (3) a part soaks downward 
into the ground where it is retained for a longer or shorter 
period. 

*Different views are held as to the origin of Underground waters, 
for while it is generally conceded thit the rainfall is the chief 
source, some believe that the original constituent water of the igne- 
ous rocks is the source of certain highly carbonated springs. Others 
think that the sea water included in marine sediments at the time 
of their accumulation is the source of some saline waters. 



DISPOSITION OF WATER FALLING UPON LAND SURFACE. 33 

(i) Evaporation before absorption. — During and immedi- 
ately following- precipitation in the form of rain, the atmosphere 
is' commonly nearly or quite saturated with vapor, and the 
evaporation which takes place before the rain is absorbed by 
the ground is very small, the amount being practically negli- 
gible as compared with that absorbed by the soil and later evap- 
orated from its surface or through its vegetation. The evap- 
oration from the streams in a region like Alabama, though con- 
siderable in the aggregate, is also small as compared to that 
from the general land surface after absorption, probably not 
averaging more than i or 2, possibly 3 per cent, at the out- 
side, of the whole amount evaporated. In broad general com- 
putations, the entire evaporation proceeding the absorption of 
the Avater by the soil may be neglected without introducing any 
material error. 

(2) Direct runoff of Flood flow. — This portion of the rain- 
fall makes its way by open channels into the streams and thence 
finally back into the ocean, in its progress carving and sculp- 
turing the land surface into irregularities which constitute scen- 
ery, and producing the infinite variety of topography which we 
everywhere see. It moves the loos'e rock waste down the slopes 
and into the streams where, reinforced by seepage waters, it 
carries the waste, often after many interruptions, finally into 
the sea, and spreads it upon the sea bottom in layers of sorted 
materials, the basis of a new series of rock formations', which 
may be added to the dry land by the uplifting of this sea bot- 
tom. Held back temporarily in its descent by more resistant 
rock ledges, it develops power which may be utilized by man ; 
in other parts, where unobstructed, it is available as a means 
of transport ; when occasion demands' it may be stored up by 
artificial means and used for power, for irrigation, and for 
other purposes. 

Few observations have been made as to the amount of water 
which thus passes from the land without being first absorbed, 
but this is known to be very small when any large district is 
considered. In a sandy soil only 3 or 4 per cent of the rainfall 
may be thus returned. On the other hand Prof. Prestwich*, 
for a region showing an ordinary succession of permeable 

*Geology, Vol. I, p. 155. This assumption is probably consider- 
ably too large. 
3 



84 GENERAL DISCUSSION OF UNDERGROUND WATERS. 

strata, assumes that 1-3 of the total rainfall is removed by di- 
rect runoff. In certain limited glacial areas, where the rocks 
are nearly or quite free from soil, this percentage of direct run- 
off may be much greater than this' amount. In the Coastal 
Plain region of Alabama perhaps one fourth of the soil is clayey 
and would have a runoff as high as that indicated by Prof. 
-Prestwich, but the remaining three-fourths are sandy and 
should possess a direct runoff of less than 5 per cent. It is 
believed that' the direct rurfbff in the area of the consolidated 
rocks in the northeastern portion of the state will not average 
more than 15 or 20 per cent of the rainfall. 

(3) Absorption. — Neglecting the small amount of evapora- 
tion taking place before absorption and deducting 15 per cent 
of the total rainfall to cover the direct surface runoff, we have 
a total of approximately 85 per cent, of the rainfall absorbed 
by the soil. 

This absorbed water plays an important part in the disinte- 
gration of rocks and their conversion into soil. It takes up the 
soluble matters encountered in its pas'sage through the rocks 
and soil, transporting a part of them in solution to the sea, de- 
positing a part in the interstices of loose sediments cementing 
them into rocks, concentrating and depositing another part in 
veins or beds or other available forms in which they may be 
turned to the use of man. It maintains and regulates' the sup- 
ply of moisture in the soil, without which all vegetable life 
would be impossible. It saturates the soil below certain depths, 
affording thus the sources of our springs and wells ; and by 
its slow but constant movement through the ground it feeds the 
streams as they flow towards the sea. 

A large amount of it is returned to the atmosphere by evapo- 
ration either directly from the surface and through the tissues 
of growing plants, or from the streams after the surplus of 
the ground water has joined them by seepage. In Alabama the 
evaporation, owing to the limited area exposed in proportion to 
the length of the drainage systems and to the humidity of the 
climate, is not especially high. Determinations made in the 
years' 1900-1903 of the runoff of the Alabama river, showed that 
27 of the 54 inches of rainfall were returned by the stream to 
the sea, most of the remaining 27, or nearly 50 per cent, of 
the rainfall, having been lost by evaporation. 



AMOUNT OF WATER AVAILABLE TO ARTESIAN WELLS. 35 

Over the broad area of the Mississippi basin the average 
evaporation is much greater. According to Messrs. Humphries 
and Abbott* only 25 per cent, of the total rainfall of this basin 
is discharged into the Gulf of Mexico. Nearly 75 per cent, 
must, therefore, have been lost by evaporation. 

Final Runoff. — One per cent, or less of the water remaining 
after evaporationt may be taken up in chemical combination by 
the rocks; the rest representing about 35 per cent, of the total 
rainfall, joins the permanent underground water body occupy- 
ing the pores of crevices within the rocks and other materials 
below the water table. These materials in the course of time, 
where conditions have been favorable to the absorption, have 
become filled to saturation, so that at the present time practically 
all of the ground water not lost through evaporation finds its 
way by seepage into the streams, constituting at least two-thirds 
of what is ordinarily spoken of as the final run-off, the other 
third being contributed by the surface run-off or flood flow. 

It is in high degree probable, however, that the direct sur- 
face run-off in Alabama covers less than 15 per cent, of the 
rainfall, and that the proportion of the final run-off contributed 
by underground seepage is' correspondingly greater than above 
given. 

AMOUNT OF WATER AVAILABLE TO ARTESIAN WELLS. 

It is computed that one inch annual rainfall amounts to 17,- 
378,743 gallons 1 per square mile; 52 inches, which is the average 
rainfall for the State of Alabama, being thus equivalent to 903,- 
694,636 gallons to the same area. Since the area of the State, 
according to the Twelfth Census, is 52,250 square miles, the 
total rainfall per annum for the State amounts to 47,218,044,- 
731,000 gallons'. 

As we have seen above, approximately 85 per cent, of this 
rainfall is' absorbed by the ground. This amount is equwalsnt to 
a daily supply of 109,959,830,195 gallons for the whole area, 
or 2,104,494 gallons daily per square mile. 

*Report on the Mississippi River, p. 132. 

tC. Bft Van Hise, Treatise on Metamorphism, Monograph, 47; U. 
S. Geol. Surv., p. 156. 



36 GENERAL DISCUSSION OF UNDERGROUND WATERS. 

The largest flow measured by the writer in Alabama is that 
of the great well near Roberts in Escambia county, which 
yields 5,000,000 gallons daily. The average daily rainfall 
would supply 21,992 such flows, or nearly 90,000 such as that 
of the Pickens well yielding 850 gallons per minute, provided 
all the water entering the soil were available to wells'. 

If we exclude the 50 per cent, returned to the atmosphere 
through evaporation of the 85 per cent, of the rainfall absorbed 
by the ground, there would still remain 35 per cent, theoretical- 
ly available ; but as a matter of fact the clays and other of the 
finer soi 1 s may contain a large amount of water and yet be- 
cause of their compactness give up a little of it to wells pene- 
trating them. For this reason the amount of available water 
may fall far short of the maximum above given. 

These rough estimates given, even with the limitations men- 
tioned, will suffice to show that the rainfall is adequate to sup' 
ply as many artesian wells as are likely to be sunk within the 
limits of the State supposing them to be evenly distributed 
over the area. 

As a matter of fact, however, the wells are at present, and 
probably always will be, more or less concentrated in groups 
which may lead to an excessive draining on the resources' of 
certain districts. 

It may be remarked that the water which soaks into the 
ground, passes directly downward into the artesian reservoir 
rather than laterally toward the stream channels, and that an 
excessive drain on account of artesian wells would show its'elf 
first of all in the general lowering of the water table, with con- 
sequent diminution of the supply of water in shallow wells and 
springs, and in the lessening of the run-off of the streams. 

We may therefore be safe in saying that so long as' the shal- 
low wells and springs continue to yield, and so long as the 
streams continue to flow, our artesian supply may be counted 
on. 

DEPTH OF PENETRATION. 

The downward penetration of water under the influence of 
gravity takes place through cracks and fissures or through 
pores of the rocks, and its' lower limit will be reached when 
these openings no longer exist. The depth at which all pores 



MOVEMENTS OF UNDERGROUND WATERS. 37 

are closed has been estimated to be about six miles. Experi- 
ence, however, shows that ground waters do not actively cir- 
culate to any such depth, being confined in fact largely to the 
upper 2,000 feet of the crust where they occur mainly in sed- 
imentary rocks. In crystalline rocks' the depth to which the 
water pentrates in economic amounts is usually much less, 
few wells obtaining supplies at depths of more than 500 feet. 

DISTRIBUTION AND MOVEMENTS OF UNDERGROUND 
WATERS. 

Underground water, like that which circulates in the ocean 
and in the atmosphere, is in constant motion as observation 
shows'. The chief cause of this motion is gravity. Capillary 
action and thermal changes are effective also, but in compara- 
tively limited degree. 

The distribution of the ground water and the direction and 
other peculiarities of its movements are in so great measure 
determined and controlled by the physical structure and ar- 
rangement of the materials through which it circulates, and by 
the surface topography, that a consideration in some detail of 
these modifying causes' becomes necessary. 

Modifications of Groundwater Movements due to 
Physical Structure. 

porosity. 

All the materials, whether loose or consolidated, composing 
what is commonly called the curst of the earth, are in varying 
degree capable of absorbing water through the pores or open 
spaces separating the particles. The degree of porosity is de- 
termined by the size and shape of the particles' and their close- 
ness of approximation. If the particles are of somewhat uni- 
form size and shape, and rounded, the porosity will vary be- 
tween 25 and 45 per cent, according to the closeness of the 
packing. In material composed of grains of varying size and 
shape, the porosity is considerably less. 

Thus the residual materials resulting from the weathering of 
crystalline rocks and consisting of grains varying perhaps from 
a quarter of an inch in diameter down to the finest clay, would 



38 GENERAL DISCUSSION OF UNDERGROUND WATERS. 

absorb much less water than if the grains were of uniform 
size, whether like the larger grains or the smaller. Neverthe- 
less, because of the looseness of such materials the porosity 
may be as high as 30 per cent, or more of the volume. 

In sedimentary deposits (mechanical), the materials are 
more or less completely sorted according to the weight of the 
individual particles, and hence the different beds of this kind 
are likely to be composed of grains of approximately uniform 
size, and in the unconsolidated condition may possess a poros- 
ity amounting to 20 to 50 per cent, of their volume. 

The calcareous sediments formed by the precipitation of car- 
bonate of lime by organic agencies' may be in the form of lime- 
stones or of a calcareous ooze or mud, originally as open and 
porous as the mechanical sediments above considered, but more 
liable to have the pores filled by secondary deposition of car- 
bonate of lime, and to become compacted limestones, which 
are' at times the most impermeable of rocks. Under certain 
conditions, however, in the form of chalk or chalky marls, 
these beds may retain their porosity. In the change from lime- 
stone to dolomite the rock becomes open-textured because of 
shrinkage in volume, and the permeability of all rocks may be 
increased by the formation of cracks and fissures from any 
cause. 

On the other hand the porosity of loose and open-textured 
sediments may be diminished by pressure, and by secondary 
filling of the pore spaces. So while all the rocks exposed at 
the surface of the earth or lying within a few miles depth from 
the surface, possess' a greater or less degree of porosity, this 
porosity diminishes with the depth from the surface and is 
practically nil long before the extreme depth of five or six 
miles is reached, at which theoretically the existence of open 
spaces becomes impossible. 

Amount of water absorbed by porous rocks. — The porous 
beds above referred to, in a region of adequate rainfall, below 
the water table will be saturated with water to a very consid- 
erable depth, and the amount of water thus absorbed is very 
great, as will be apparent when we consider that over 90 per 
cent, of the surface of the earth is occupied by such beds. In 
general the compact rocks' show rarely over 15 per cent, of 
pore space, but one hundred feet thickness of rocks of this 



MODIFICATION OF GROUNDWATER MOVEMENT. 39 

degree of porosity, when saturated with water would hold an 
amount equivalent to an underground lake of water 15 feet 
deep. In one hundred feet thickness of loams and clays and 
chalks similarly saturated, the amount would be correspond- 
ingly greater. 

In the following table are given the amounts of water which 
a cubic foot of some common materials will absorb.* 

Comparative Absorptive Capacity of Different Materials. 



Water ab- 

Material sorbed pe: 

cubic font 



Water ab 
Material sorbed per 

cubic foot. 



Quarts. I Quarts. 

Sand 10 'Dolomite 1 to 10 

Potsdam sandstone 2 to 6 ;Chalk 8 

Triassic sandstone 4 Granite 1/100 to, 14 

Trenton Limestone y± to l 1 ^ 

Incomplete Saturation : — It is generally assumed as above 
stated, that below the water table and down to the limit of 
meteoric circulation, the pores of all the strata are filled to 
saturation with water. But recent studies of well records 
and samples have shown that this is far from being true.t 
"Few of the crystalline rocks, for instance, hold anything like 
their full capacity of water. Many mines in both sedimentary 
and crystalline rocks are dry and dusty even when far below 
the water level, open and porous sandstones which contain no 
water at all have been recognized in deep wells, while clays 
underlying the ground water are often incoherent and pow- 
dery. Estimates' of the ground-water in the earth have varied 
many hundred per cent, because of the different initial assump- 
tions made in the computations." 

Lost Water. — -This phenomenon also is referred to in the 
article above quoted. "Many of the iower sandstones of south- 
western Pennsylvania and elsewhere, although open and po- 
rous, are found by the drill to be destitute of water. That they 
are beyond the ordinary limit of meteoric circulation will be 
admitted,' but as marine formations', they must have been sat- 
urated at the time of their deposition, and as they have never 

*M. L. Fuller Water Supply Paper No. 114, U. S. Geol. Surv., p. 23. 
fM. L. Fuller, Economic Geology, Vol. I, page 5G5. 



40 GENERAL DISCUSSION OF UNDERGROUND WATERS. 

down to the present time been above sea or drainage level 
the water should, in the absence of any known means of escape 
still be present. This, as has been indicated, is not the case. 
The problem of what has become of this water is one of the 
more fascinating ones' left for future solution." 

PERMEABILITY. 

Marked differences exist in the rate of movement of water 
through permeable rocks. Falling upon sand water is quickly 
absorbed and transmitted through the relatively large pores to 
the permanent groundwater below, and a small proportion only 
is lost by evaporation or direct surface runoff. In the case of 
clays the water penetrates the capillary pores very slowly. 
The pores in the upper layers soon become filled and much 
water is lost by direct runoff and by evaporation because of 
the slowness with which it penetrates the underlying layers. 
Thus, while clay possesses high absorptive capacity it holds 
water with wonderful tenacity, and offers the greatest resist- 
ance to any movements through its pores. 

For these reasons clays are clas'sed with the impervious ma- 
terials, and in most of the artesian systems of Alabama, serve 
as the water-tight confining beds to the water-bearing sand- 
stones and other open-textured rocks. Of course, with suf- 
ficient time the water taken up by the clay will be transmitted, 
but this movement is so slow that for our present purposes it 
may be ignored. 

Other fine grained materials exhibit similar qualities and 
Professor Prestwich* has shown that some chalks, with the 
same absorptive capacity as certain sandstones, transmit water 
600 times slower. 

Cause and rate of ■movement of underground waters.— 
Gravity is the chief cause of the movements of underground 
waters as' it is for the movements of water in the surface 
streams. In both cases the flow is from a higher to a lower 
level. The rate of movement, according to Schlichter,t de- 

*Geology, Chemical, Physical, and Stratigraphic, Vol. I, page 159. 

fThe Motions of Underground "Waters; "Water Supply Paper No. 
67, U. S. Geological Survey, p. 17. 



MODIFICATION OF GROUNDWATER MOVEMENT. 41 

pends (i) on the size of the pores, (2) on the degree of po- 
rosity, (3) on the pressure, and (4) on the temperature. 

Ve'.ocily. — According to this author the velocity of the 
groundwater flow is the rate (measured as so many feet a day, 
or a year, etc.,) at which the water advances through the 
porous medium, irrespective of the amount of water thus' ad- 
vancing. For materials of various grades the following re- 
sults have, heen obtained : 

Velocity of Groundwater through Materials of different Grades, 

having a Pressure Gradient or Slope of 10 Feet 

to the Mile. 

Material. 

Fine ssnd 0.2 mm. diameter 

Medium sand 0.4 mm. diameter 

Coarse sand 0.8 mm. diameter 

Fine gravel 2 mm. diameter 

The velocity for any other gradient can easily be calculated 
from the above. Thus, for a gradient of 100 feet to the mile, 
the velocity will be ten times that given in the table. 

Flow or Discharge. — The amount of water (measured in 
cubic feet per minute) passing through a given cross section, 
is called the flow or discharge, and for the same materials and 
same degree of porosity and same gradient as in the preceding 
table, this flow is shown in the following table : 

Flozv of Ground-water in Materials of different Grades, through 

a Bed of Vertical Cross section 200 by 1000 Feet, 

sloping 10 Feet to the Mile. 



Miles per year. 


Ft. per year 


0.010 


52.8 


0.041 


216.0 


0.16 


845.0 


1.02 


5,386.0 



Cubic ft. per minute. 

Fine sand 5.5 

Medium sand 22.0 

Coarse sand 87.0 

Fine gravel 546.0 



When the results of experiments on loose unconsolidated 
materials are compared with the actually measured rate of 
flow through the rocks for long distances, great discrepancies 



42 GENERAL DISCUSSION OE UNDERGROUND WATERS. 

appear ; for it is found that the flow through rocks is many 
times more rapid than the calculated and observed movements 
through porous sands'. Concerning this Professor King* says: 

"It appears clear therefore, that the movements of 

water across long distances must take place in considerable 
measure through passage ways larger than those which de- 
pend upon the pore space fixed by the diameters of the grains 
which constitute the beds' themselves." 

There is no doubt but that the rate of flow of water through 
the superficial layers' of rocks is increased by the existence of 
cracks and fissures due to the contraction and expansion from 
changes of temperature, to frost, crustal movements, etc., but it 
must be borne in mind on the other hand that at considerable 
depths below the surface these cracks and fissures are likely to 
be closed by the creep of the rock, and by the deposition of 
mineral matters' from the circulating waters, so that after all 
we may conceive of the transmission of water through the 
rocks, and especially through deep seated rocks, as being main- 
ly through the pores of the rocks themselves. 

We have heretofore taken no account of another factor 
which ; s bound to affect the rate of flow, viz., hydrostatic pres- 
sure. On this point Prof. W. H. Nortont says, "rocks which 
transmit but feebly at the surface yield water at far greater 
ratios under strong pressure of artesian head. Since one pound 
of pressure to the square inch is required to support each 2.31 
feet of water, in a flowing artesian well 1,155 ^ eet deep in 
which the water rises to the surface from the bottom of the 
well, the water must exert at the base of the boring a pressure 
of 500 pounds to the square inch. The effect of such pressures 
must be to augment greatly the horizontal transmis- 
sion of water. The effect of even a moderate increase of pres- 
sure is' seen in mechanical filters, and the rapid rise in perco- 
lation accompanying the use of such pressure is set forth in 
certain experiments made by Isaac Roberts. $ The stone 
through whose pores the water was forced is stated to have 
been to 10 1-2 inches thick, and of "average coarseness." 

*Nineteenth Annual, U. S. Geol. Survey, Part II, page 249. 
fArtesian wells of Iowa, Iowa Geological Survey, Vol. VI, page 
165. 

|De Ranee, Water Supply of England "Wales, p. 19. 



MODIFICATION OF GROUNDWATER MOVEMENT. 43 

Relation of Percolation to Pressure. 

Pressures. Percolation. 

10 pounds to square inch 4 y 2 Imperial gallons. 

20 pounds to square inch 7 V 2 Imperial gallons. 

40 pounds to square inch 19 Imperial gallons. 



The temperature of the water is also an important factor in 
determining the rate of flow, the movement being noticeably 
greater for high temperatures' than for low ones, as shown in 
the following table.* 

Relative Flow of Water at various Temperatures through Soil. 
(Standard Temperature is 50 Degrees F.) 



Relative Relative Relative 

Temperature flow. Temperature flow. Temperature flow. 
Degrees F. Degrees F. Degrees F. 



32 


0.74 


55 


1.08 


80 


1.51 


35 


0.78 


60 


1.16 


85 


1.62 


40 


0.85 


65 


1.25 


90 


1.70 


45 


0.92 


70 


1.34 


95 


1.80 


SO 


1.00 


75 


1.42 


100 


1.90 



Modifications of Groundwater Movement due to 
Topography. 

The running streams found in the caverns and subterra- 
nean channels' of limestone formations, and in less degree in 
the cracks and fissures of other rocks, while sometimes of large 
size and of local importance, form but an insignificant part of 
that great body of water circulating through sands, and other 
porous strata, with which we are here chiefly concerned and 
which is here termed "ground water." 

GROUNDWATER DIVISIONS. 

In the discussion of underground waters three divisions have 
been recognized: (1) The unsaturated zone, (2) The sur- 
face zones of flow, and (3) The deep zones of flow. 

*Schlichter Water Supply Paper, No. 67 U. S. Geol. Survey, p. 24. 



44 GENERAL DISCUSSION OF UNDERGROUND WATERS. 

The unsaturated zone extends from the surface of the 
ground down to the upper surface of the groundwater body — 
"the water-table." In this zone the saturation of the strata is 
prevented partly by the downward percolation of the water 
into the permanently saturated layers and partly by its' being 
brought back to the surface by capillarity and the roots of 
plants and there evaporated. 

The surface zone of flow extends from the level of the water 
table clown to the first impervious stratum of considerable 
extent. The deeper zones of flow are those which lie below the 
first impervious stratum, and of these there may be several 
in the same region. 

In the discussion of artesian systems we shall be chiefly con- 
cerned with the deeper zones of flow, while most of the other 
problems of the water supply pertain to the surface zone. 

Surface Zone of Flow, 
form of the groundwater table. 

The upper surface of the groundwater body, or the water 
table, shows a general agreement with the surface configu a- 
t ; on of the land. Where the surface is horizontal over any 
broad area the water table likewise tends to be horizontal, its 
distance below the top of the ground depending partly on the 
rainfall and partly upon the depth from which moisture can be 
raised to the surface and evaporated. Where the land is 
sloping the water table slopes in a similar direction but usually 
at a less angle. Again where the surface is hilly there are 
corresponding but less marked undulations in the water table, 
the latter being practically at the level of the streams in the val- 
leys, while under the crests of the hills it is considerably be- 
low the surface, the distance depending upon the arnount of 
rainfall and the angle o* slope towards the valley . 1 aese re- 
lations are very well shown in the accompanying diagram taken 
from Schlichter. 



MODIFICATION OF GROUNDWATER MOVEMENT. 



45 




Pig. 3. Ideal section across a river valley, shewing the position of 

the groundwater and the undulations of the water table with 

reference to the surface of the ground and bed rock. 



Ordinarily the surface of the water tab'e is above the level 
of the streams, and it will easily be seen how streams' are con- 
stantly fed by seepage from the higher lands on each side, and 
how valleys not occupied by streams may be kept wet by the 
slow rise of water from below as it is forced up by hydrostatic 
pressure. This will be illustrated by the subjoined figure.* 



'.:;;; 



Original wattrtatli 



Fig. 4. Diagramatic section illustrating seepage and the growth 
of streams. Lines with arrows are lines of flow. 



This figure will also show that the very general belief that 
underground waters are fed from rivers and lakes, is true 
only in very exceptional cases and under peculiar circumstan- 
ces, for the hydrostatic pressure forcing the water from the 
highlands into the stream will in most cases exceed the pres- 
sure in the opposite direction. 

Where, however, shallow soil is spread out over limestones 
cut by fissures and cracks, it may happen that the groundwater 
level cannot be maintained above the ordinary level of some 
of the surface streams. Similar conditions may exist in certain 
porous sandstones or other fissured rocks which are deeply 
underdrained. Again, in the arid region streams flowing out 
upon dry plains over channels of coarse materials, are often 



*Schlichter Movements of Underground Water. 
Paper No. (57, U. S. Geological Survey, p. 13. 



Water Supply 



46 GENERAL DISCUSSION OE UNDERGROUND WATERS. 

rapidly absorbed, the water joining' the so-called 'underflow' 
which may emerge further down the valley. 

Usually this underflow is not important, yet where the river 
slope (downstream) is great and the material deposited in the 
river channel is coarse, or where the fine silt of the channel 
covers deeper deposits of coarser material, rendering seepage 
into the channel difficult and underground passage downstream 
easy, the underflow may be relatively large, but the velocity 
of the underflow is always, according to Schlichter, very small 
and the total amount is' commonly greatly exaggerated. 

The depth of the water table, as we have seen, is greatly 
influenced by topography, but in regions of abundant rain- 
fall and comparatively little evaporation, as in the eastern 
United States, the permanent groundwater level is seldom very 
far below the surface even in the uplands. In most parts of 
the Alabama highlands wells do not require to be more than 
ioo feet deep, and water is usually obtained at a much less 
depth. In lands of medium elevation the usual depth of wells 
is from 30 to 40 feet. In the valleys and low grounds water 
is often obtained very near the surface, and usually at depths 
of from 10 to 15 feet. It is only in the arid regions of the 
country that the groundwater level is many hundred feet below 
the surface. 

Modifications oe Groundwater Movement due to 
Stratification. 

Deep Zones of Flow. 

The materials of sedimentary formations are more or less 
perfectly sorted according to size, and the strata of different 
kinds constituting a cycle of deposition, normally succeed each 
other m a definite order, which is, pebbles and coarse sands be- 
low, followed in ascending order by finer sands, and these in 
turn by clays. To these inorganic matters' must be added, as 
the last term of the series, the organic sediments, chalk and 
limestone. 

Of the sediments above named the sandstones or sands 
usually constitute the porous, permeable beds, and the shales' 
or clays, the impervious ones. The limestones in general may 
be classed as impervious, but some of the chalks, and especially 
those limestones, which are made up of loosely cemented frag- 



MOVEMENTS OF UNDERGROUND WATERS. 47 

ments of shells and those which by exposure to weathering 
in the unsaturated zone, have become fissured and traversed 
1>\ caverns and other open passage ways, may be in very high 
degree permeable, and thus water-bearers. Of this nature are 
the loose textured, shelly limestones of the Claiborne formation 
which constitute the water-bearing stratum of so many arte- 
sian wells in Georgia, Alabama, and Mississippi. In still 
another way limestone may become open-textured, viz., in its 
alteration into dolomite, with attendant diminution in volume, 
and development of cracks and interstices. 

In any considerable thickness of stratified deposits represent- 
ing a number of cycles of deposition as above outlined, there 
will almost certainly be found beds of porous materials well 
fitted for quickly absorbing water and for transmitting it by 
percolation, enclosed between beds which are relatively im- 
pervious. And since these beds are nearly always inclined at 
some angle to the horizon they furnish the conditions for 
storing, and maintaining a circulation of water far below the 
zone of surface flow in one or more systems or zones of deeper 
flow as defined above. 

The distinguishing features of the deeper zones of flow have 
been so clearly presented by Prof. Schlichter in the work so 
often referred to above, that we can not do better than quote 
his words. 



"The pervious and water-bearing sandstones and limestones be- 
neath the surface zene of flow constitute what we have called the 
deeper zones of flow. There may be several of these deeper zones 
or they may be absent altogether. When present, they may be dis- 
tinguished from the surface zone of flow by the following character- 
istics: 

(1) The surface zene of flow has a free, unconfmed upper boun- 
dary (the water table) and an impervious lower boundary. Tha 
deep zone of flow has an impervious upper boundary as well as an 
impervious lower boundary. 

(2) The unit of the upper zone of flow is the drainage area or 
river valley. The unit of the deep zone of flow is regional and 
geologic and not dependent upon surface contours. However, it 
must not be forgotten that the deeper geologic structure is fre- 
quently the principal determining factor controlling the surface 
drainage, so that the deep zenes of flow do not commonly run 
counter to the direction of the surface flow. 

(3) The surface zone of flow is dependent upon the local rain 
fall of the immediate region. The deeper zones of flow receive their 
waters from distant areas. 



48 



GENERAL DISCUSSION OF UNDERGROUND WATERS. 



(4) The surface zone of flow is in part above the level of surface 
drainage channels, while the deeper zones are entirely below the lo- 
cal drainage level. 

(5) There is commonly a difference in the chemical composition 
of the waters from the two zones. It is difficult in our present state 
of knowledge to make valuable generalizations. The waters oi 
the surface zcne are usually less mineralized than those of deep 
strata, but in arid regions this general rule is frequently reversed. 
The carbonates are the predominant salts of the surface waters 
The deeper waters are usually characterized by rather high amounts 
of dissolved chlorides. "Waters of the suiface zone contain dis- 
solved oxygen gas, which is almost entirely absent from the deep 
waters."* 

RECOVERY OF UNDERGROUND WATERS. 

Water is returned to the surface mainly by two general 
ways: (i) By springs', and (2) by wells. 

Waters Near the Surface. 

Springs. — It has already been pointed out how in a region of 
uneven surface the rain-fall soaking into- the ground will raise 
the level of the groundwater in the uplands until the head is 
sufficient to cause lateral movement towards the low ground, 
where it will rejoin the surface water by general seepage or 
seepage springs along the sides of the valleys, or pass into lakes 
and running streams and even into the sea if the distance is 
not too great. Where the emergence of the water is concen- 
trated in a small area we have what is known as a spring. 
Such springs most commonly emerge just above an impervious' 
bed. (Fig. 5)t or from between two impervious beds. (Fig. 
6.)t 




Fig. 5. Hillside spring from unconfined water bed without head. 



*The Motions of Underground Waters, page 53. 

fM. L. Fuller. Water Supply Paper, No. 145. U. S. Geol. Survey: 
page 47. 



RECOVERY OF UNDERGROUND WATERS. 



49 




Fig. 6. 



Hillside spring from confined water bed under more or 
less head. 



In limestone regions they generally emerge from solution 
passages in a mass of uniform rock. These are often of con- 
siderable size, and are commonly known in Alabama as "big" 
or "limestone" springs. One of the best known springs of 
this character in the State is that at Huntsville, (See Plate II). 
The water emerging from ""he subcarboniferous limestone at 
this' point forms a stream of considerable size. The Knox 
Dolomite, another extensive calcareous formation in Alabama, 
affords hundreds of similar big springs. In the Coastal Plain 
region, especially in Barbour and Plenry Counties, the Clayton 
and Nanafalia limestones, and further south the St. Stephens 
limestone of the Tertiary, are also characterized by similar 
springs. 

Open wells. — To supplement these-natural modes of recovery 
of underground waters, recourse has been had from the ear- 
liest times to artificial contrivances, the most important and 
most commonly used of these being the ordinary open well. 
An excavation is made in water-bearing sands to some depth 
below the water table. A lowering of the water table around 
the well at once follows by reason of the converging flow of the 
underground waters into the well. If the water is not drawn 
from the well the level of the water table will be restored after 
a time and stand at the same height in and near the well as 
father away. If the water be removed in any considerable 
quantity, the level of the water in the well will remain below 
that of the general water surface outside, the depression de- 
pending on the quantity of the water removed. 

Driven ivells. — The driven well is merely a modification of 
the open well, made by driving a pipe with open end, or better 
4 



50 GENERAL DISCUSSION OE UNDERGROUND WATERS. 

with closed point at the end and with perforations above it 
to admit the water. 

From the open well the water is raised by bucket, or pump, 
or other mechanical means. For a driven well the pump is 
mostly used. 

In all parts of Alabama, except in some of the limestone re- 
gions and. the Post Oak Flatwoods', (and even in these in 
places), water may always be obtained by sinking wells to 
depths varying from a few feet to one hundred or more, gen- 
erally less than fifty feet. In residual accumulations, (i. e. 
those resulting from the decomposition of the rocks ), such as 
are common in the area of the crystalline rocks, and in 
the Coal Measures, and in some limestone regions where thes'e 
surface matters are more or less clayey and localized in ex- 
tent, the supply is likely to be uncertain, and the wells to go 
dry or to diminish greatly in summer. But where the surface 
materials are of such wide distribution and of such favorable 
composition as' are afforded by the Lafayette beds that have 
been spread so generally over the whole Coastal Plain Region 
of Alabama, the supply seems to be never-failing under pres- 
ent climatal conditions. 

It is not an uncommon circumstance in some parts of the 
Coastal Plain Region, that of two. closely contiguous wells the 
water of the one may be good while that of the other may be 
unfit for use by reason of excess' of organic matter ar\d iron 
salts. The one penetrates into a buried slough or other de- 
posit of organic matters, while the other does not. This is 
shown by the accompanying figure taken from Water Supply 
Paper No. 145, U. S. G. S. page 112. 




' '!vA$.'y '£&••' 



Fig. 7. Diagram showing buried sloughs. Wells at a and b would 

furnish water containing iron and organic matter. The well 

at c would furnish comparatively pure water. 

(After Purdue.) 

Inasmuch as' the lowering of the groundwater level in the 
uplands by drainage into the lowlands, goes on very slowly, 



RECOVERY OF UNDERGROUND WATERS. 



51 



the time of low water in the wells rarely coincides with the 
season of dry weather. 

The hillside springs are subject to like conditions or limita- 
tions, they go dry in many places in the Coal Measures and 
region of the Crystalline rocks, while they are never-failing 
in parts' of the Coastal Plain where the materials of the Lafay- 
ette form the surface. 

Deep-seated Waters. 

It has been shown above how alternations of the permeable 
and impervious strata of the sedimentary formations afford the 
conditions for deep seated flow of underground waters. From 
these deeper zones of flow as from the surface zone, the water 
may also be recovered through the agency of gravity supple- 
mented by natural or artificial return ways. 

Deep Springs (Fissure springs.) — The groundwater in gent- 
ly dipping porous beds enclosed between impervious ones, 
may in the course of its downward percolation to considerable 
depths, meet with joints or fissures in the impervious overlying 
bed and thus escape to the surface, sometimes at considerable 
distance from the place at which it entered the ground, as is 
shown in the accompanying figure. 




Figure 8. Fissure spring. 



The waters of springs of this kind having been long in con- 
tact with the strata are likely to be highly charged with min- 
eral matters that have been taken into solution on the way. 
Deep springs are usually distinguished from surface spring? 
by a greater constancy of flow, by relative uniformity of sum- 
mer and winter tenperatures, and by freedom from contami- 
nation. 

Artesian wells. — In this paper the term "artesian" is used 
for any well sunk into a deep ,zone of flow where the water i- 



52 ARTESIAN WELLS. 

found under hydrostatic pressure, so that it will rise in a weti 
above the impervious confining strata. As thus defined arte- 
sian wells may be divided into flowing and non-flowing. This, 
however, is a non-essential distinction, since of two wells sunk 
into the same water-bearing stratum one may' flow while the 
other on somewhat higher ground may not. From such wells 
the deep seated waters are recovered either by natural flow 
or by pumping at the surface. 

B. ARTESIAN WELLS. 

Artesian wells are governed by certain laws and present cer- 
tain definite features, a discussion of which will be found in 
the following paragraphs. 

ESSENTIAL CONDITIONS. 

In his treatise entitled, The Requisite and Qualifying Con- 
ditions' of Artesian Wells, *Prof. Chambcrlin enumerates the 
following seven prerequisites : 

i. A pervious stratum to permit the entrance and the pas- 
sage of the water. 

II. A water tight bed below to prevent the escape of the water 
downward. 

III. A like impervious bed above to prevent escape upward, for 
the water, being under pressure from the fountain head, 
would otherwise find relief in that direction. 

IV. An inclination of these beds, so that the edge at which the 

waters enter will be higher than the surface at the well. 

V. A suitable exposure of the edge of the porous stratum, so 
that it may take in a sufficient supply of water. 

VI. An adequate rainfall to furnish this supply. 

VII. An absence of any escape for the water at a lower level 
than the surface at the well. 

These have commonly been accepted as essential to arte- 
sian flows, but recent investigationst indicate that artesian 
flows may take place where the first four of these conditions, 

*Fifth Annual Report. U. S. Geol. Survey, 1885, pp. 131-173. 

fM. L. Fuller. Artesian Flows from Unconfined Sandy Strata; 
Engineering News, Vol. 52, pp. 329-330. 



ESSENTIAL CONDITIONS. 53 

supposedly indispensable, are absent. The following figure 
representing- a typical East and West section across the bays 
on the north shore of Long Island, illustrates one such case, 
where, notwithstanding the permeability of the sands, wells' 
penetrating below the water table at the base of the bluffs 
obtain flowing- water. 




Fig. 9. Section showing conditions furnishing flows from un- 
confined sandy strata. (After Fuller.) 

Slight difference in the degree of porosity of the sands may 
account for the phenomena, or the horizontal arrangement of 
the grains, even in uniform sand, may so oppose the passage 
of the water that it will pass upward through the well with 
greater ease than through the sand of the nature described, and 
a flow will result. 

In the region of the metamorphic and igneous rocks also, 
artesian wells are obtained where some of these "essentials" 
appear to be wanting. 

In fact, adequate rainfall, suitable outcrop of the porous bed, 
and absence of leakage being assumed, it is probable that the 
one essential pre-requisite of an artesian flow is a sufficient 
difference in the level of the water table in closely adjacent 
regions. 

In the great majority of cases, however, with which we in 
Alabama are concerned, the conditions governing the artesian 
problems are practically those discussed by Prof. Chamberlin, 
and a statement of some of the most important of these condi- 
tions will help to a proper undertaking of much that follows. 

Artesian system. — A series consisting of a porous or per- 
meable bed enclosed between two impervious ones', all having 
a moderate dip or incline somewhat greater than the general 
slope of the surface, constitutes an artesian system. Water 
falling as rain upon the outcropping edge of the permeable bed 



54 



ARTESIAN WELLS. 



will be absorbed by it, and by the force of gravity will perco- 
late through it in the only direction possible, i. e. down the 
dip, general diffusion being prevented by the under-and over- 
lying impervious beds 1 . Carried thus between impervious 
sheets to a lower level than the outcrop, the water will accu- 
mulate under hydrostatic pressure, and if the overlying retain- 
ing bed be pierced by an opening, natural or artificial, the 
water will ascend, approximately to the level of its head, which 
is the outcrop of the permeable bed. 

The ideal arrangement of the strata, rarely realized in nature, 
is that in which the basin shape is approximated. In this case 
the water falling upon the outcropping edges of the porous 
beds, gradually sinks from every side toward the center of the 
basin. This case is illustrated by Fig. 10 below. 




Pig. 10. Ideal Artesian Basin. 

A far more common arrangement and one prevalent in the 
Alabama Coastal Plain is that where the strata all dip in one 
direction and the general slope of the land surface is in the 
same direction but at a less rapid rate. In such a system the 
character of the well, whether flowing or not, will depend upon 
the local inequalities of the surface. 

These conditions are illustrated in the following fisrure. 




Fig. 11. Diagrammatic representation of a single ar- 
tesian system, showing the influence of relative altitude in de- 
termining whether or not the well will flow. A is the porous 
water-bearing bed enclosed between impermeable ones. 
The well at a will flow, that at b on higher ground 
will not. 



ESSENTIAL CONDITIONS. 



55 



If the general slope of the land surface were in the opposite 
direction from the dip of the strata, a flowing artesian well 
would be an impossibility except under peculiar local condi- 
tions. 

The diagram below, Fig. 12, for which we are indebted to 
Mr. M. L. Fuller* illustrates a case which has come under his 
observation, where the water flows at a higher level than rhp 
outcrop of the water-bearing bed of the region, being fed, 
however, in part through a joint or fault from a higher lying- 
source. 




Fig. 12. Underground conditions in Thompsonville well. (Conn.) 

A very gentle dip of the strata is most favorable, for if the 
dip be great not only will the outcrop of the porous bed be 
narrow and its intake capacity thus reduced, but the water will 
very quickly be conducted to depths which it would be imprac- 
ticable to reach by borings. A dip of one per cent, will carrv 
a stratum down 52.8 feet in a mile ; a dip of ten per cent, will 
carrv it down 528 feet in a mile ; while a dip of 45 degrees will 
carrv the bed down one mile in a mile. These relations and 
the rapid narrowing of the area of outcrop with increase of 
the angle of the dip will be made clear by the accompanying 
diagram in which A, B and C, represent the relative widths 
of the outcrop of three strata of equal thickness but of differ- 
ent inclinations ; A at 5 degrees, B at 10 degrees, and C at 25 
degrees from the horizon. 




Fit 



Illustrating 



the influence of the dip of the strata on the 
width of the outcrop. 



*Water Supply Paper No. 110, U. S. Geol. Survey, p. 102. 



56 ARTESIAN WELLS. 

The following figures will further illustrate these points : 
A bed of iooo feet thickness inclined at different angles" 
will have a surface outcrop varying as shown in the table be- 
low. 

Angle of Dip. Width of outcrop. 

45 degrees 1414 feet. 

20 degrees 2924 feet. 

10 degrees 5780 feet. 

5 degrees 11495 feet. 

30 minutes 114547 feet. 

26 minutes (40 feet to the mile) 132275 feet. 

19% minutes (30 feet to the mile) 176367 feet. 

16% minutes (25 feet to the mile) 208333 feet. 

What has been said above refers tc a single artesian system, 
but as a matter of fact the supply of a well may come from 
more than one such system, and the motion of the water is in 
consequence far more complicated than above indicated. On 
this point Mr. King* writes as follows : 

"It would appear that all fissures of all rocks must participate in 
the horizontal movements of ground water to a considerable extent 
if they lie below the plane of saturation and are in any way con- 
nected with a water-bearing stratum. Where' two sandstone (po- 
rous) horizons are separated by rock formations possessing jointed 
structure developed in a marked degree it may be that these joints 
and fissures participate in no inconsiderable extent in the horizontal 
transmission of the water." , 

"It may also be true that such beds separating two sandstone 
formations will serve to make the water in both beds available to 
wells which penetrate only the upper horizon, the water reaching 
the well' not directly but by rising in a general way at many places 
or along numerous lines and networks of fissures and over wide 
areas, in such a manner as to keep the upper sandstone more nearly 
filled with water and thus maintain the pressure in the reck about 
the well at a materially higher point than would otherwise exist, 
especially in such cases as the wells of the city water works where 
continuous pumping is maintained." 

"It may even be true that water from an upper horizon of sand- 
stone may, in certain regions, pass through a general system of 
fissures into one of lower level, and vice versa, during the horizontal 
transmission, the water taking in all cases the line of least resistance 
so that if in the upper horizon of sandstone in a particular region 
the texture is closer than that in the lower, the general flow could 
well divide and become in one section stronger than normal, first in 
the lower horizon and then in the upper horizon, according as the 
textures of the two rocks vary in coarseness." 

"It would appear that the more rational view to take of the move- 
ment of underground water is that it is one more or less continuous 

*Nineteenth Annual Report, U. S. G. S. Part II, page 249. 



MODIFYING CONDITIONS. 57 

body receiving accessions at many high levels and discharging its 
water at many lower levels, but that the water in reaching its lower 
levels may not all of the way follow continuously one particular 
geological horizon.' 

"It is of course true that the maximum flow must be concentrated 
in the sandstone horizons, but it seems also necessary to suppose 
that even here there may be joints, fissures, or ether waterways 
which materially assist in the transmission of the water." 

"In the case of wells sunk in rock the flow of water into them may 
be very much more rapid than that of the general flow of the water 
through the formation into which the well is sunk, because when 
the water is taken out, either by pumping or by natural discharge, 
a lecal effective head is developed, much greater than the general 
effective head, and as the water approaches the well from all sides, a 
relatively very slow flow, even a few feet back from the well, will de- 
liver a large amount of water to the well, and if the material is 
coarse and the bore of the well small the amount delivered may even 
tax the capacity of the well to deliver the water which is brought to 
it." 

MODIFYING CONDITIONS. 

In a single artesian system of the Alabama Coastal Plain, 
of limited extent and fairly uniform in the composition and 
structure of its strata, the conditions will be about as repre- 
sented in the diagram given above, Fig. II. 

In the very nature of things, however, these sediments will 
not be in continuous and unbroken sheets under the whole 
expanse of the Coastal Plain. They will be intersected by 
streams and will vary in the character of the materials and 
their thickness and order of succession from place to place, 
so that wells', which from their position should have nearly iden- 
tical logs or records, do often show very great differences. 
Some of the complications thus brought about may be briefly 
noted. 

Effects of erosion. — If the water-bearing stratum be inter- 
sected by a ravine or stream valley at right angles to its dip, 
the effect on wells on the two sides of the ravine may be very 
different as the following diagram will show. 



58 



ARTKSIAN WELI 




Fig. 14.— Section shewing the effect of erosion. A is the porous 
water-bearing bed between two impervious ones. The well a will 
flow provided the distance from the ravine be considerable and the 
leakage from the water-bearing bed into the ravine not too great, but 
the well b will probably not flow because of this leakage into the ad- 
pjacent ravine. 

The well at c might not yield water if the exposure of the water- 
bearing bed was limited to the side of the ravine and therefore of 
small area, but if the bed outcrops over considerable area of the 
valley floor as shown in the figure, a flow would probably be obtained. 

Variations in the Water-bearing stratum. — In two principal 
ways the water-bearing stratum may change so as materially 
to affect the artesian prospects. It may thin down in the di- 
rection of the dip until the confining- impervious beds come to- 
gether. Above this point a well may be successful, below it not. 
Again, the porous bed may become gradually finer and finer in 
texture, or it may be gradually replaced by silt or clay, and trm*, 
the transmission of the water may be clogged or prevented. 

Conditions like these are common enough in the Coastal 
Plain region and from the very nature of the mode of accu- 
mulation of off-shore sediments, are normal, for the coarser 
materials deposited near the shore are succeeded by finer tex- 
tured sands and by silts and clays as the distance from the shore 
increases. The two figures below will illustrate these condi- 
tions. 




Pig. 15. Section .illustrating the thinning out of a porous water- 
bearing bed, A, enclosed between impervious beds B and C thus 
furnishing the necessary conditions for an artesian fountain at 
D, but to the left of D the conditions for such fountain would be 
absent. (After Chamberlin.) 



MODIFYING CONDITION'S. 59 








Fig. 16. Section illustrating the transition of a porous water- 
bearing bed A, into a close textured impervious one. Being en- 
closed between two impervious beds B and C, it furnishes the con- 
ditions for an artesian fountain at D, but not for cne to the right 
of D where the porous bed is replaced by an impervious one. (Af- 
ter Chamberlin.) 



/ 'an'atious in the confining impervious beds. — These beds 
may vary in texture from place to place, or they may be cracked 
and fissured in such a way as ta permit leakage sufficient to 
modify very materially the artesian conditions. Defects in 
the confining- bed below may allow leakage into a lower po- 
rous' bed which outcrops at a lower level, thus reducing the 
effective head of the upper water-bearer. The character of the 
confining bed above is even more important than that of the 
underlying one, for the water being under pressure will be 
forced, through it unless it be comparatively water-tight or 
else very thick, and thus the amount of water available to the 
well will be diminished possibly to the extent of preventing a 
flow altogether. 

The efficiency of the cover increases with its thickness as 
may be easily understood, and a relatively porous cover may 
under certain circumstances' not only serve as a confining bed 
but may even increase the yield of water. This will be the case 
when the surface of the country between the fountain head 
and the well is high so that the general level of the water ta- 
ble is above the outcrop of the porous water-bearing bed. 

The downward pressure of this groundwater will not only 
prevent the upward escape of the artesian water but may even 
add to its volume. 

On the other hand, if the country between fountain head 
and well is low and the cover on that account comparatively 
thin, there will be some leakage unless this cover is' exception- 
ally impervious. 

In this way the occurrence of a river valley between the foun- 
tain head and the well may seriously lessen the probabilities of 



60 



ARTESIAN WELLS. 



success of a well, even when the artesian system lies well below 
the floor of the valley and the cover is not cut by the bed of the 
stream. 

Other modifying conditions. — In a region like the Coastal 
.Plain of Alabama, which includes a number of artesian sys- 
tems, other complications arise from irregularities in the ex- 
tent and in the order and distribution of the various strata. 
The following figures, taken or adapted from Darton,* are in- 
troduced to illustrate a few of the cases commonlv encountered. 






^MXtPsm 






Mm 






Fig. 17 Illustrates the case where an impervious bed overlaps 
completely the intake area of the porous bed, thus greatly dimin- 
ishing or cutting off its water supply. This porous bed may be, at 
other points along its outcrop, bared of this impervious overlap and 
thus be water-bearing. 




Fig 18 Represents the occurrence of a gravel bed completely 
enclosed in clays so that no water can accumulate in it, and a well 
at A although finding favorable materials for water would obtain 
none. 




Fig 19 Shows the case where gravelly bedy of ancient streams 
or the beaches of ancient lakes have become buried under the later 
accumulations of impervious materials and rest on the same. Two 
of these lines of gravel, which may be narrow and sinuous but which 
may extend for miles, are here shown in cross section. Unlike the 
case represented in the preceding figure, the gravels are not com- 
pletely enclosed in clays, but in other parts of their courses are 
bared of the impervious cover and have thus become water-bearing. 
Wells at A A which go down into the ancient channels would be suc- 
cessful, while those at B and B wholly in the impervious material 
would not. 



♦Bulletin No. 138. U. S. Geological Survey. 



STRATA IN ALABAMA COASTAL TLAIN. 



61 




In Fig. 20 the conditions would appear to be favorable for water 
at A in the gravels between the upper clay beds, but the water does 
not accumulate, for it is free to flow over the edge of the clay into 
lower gravels, where it would be found in a deep well, as at B. 



ARRANGEMENT OF THE STRATA IN THE ALABAMA 
COASTAL PLAIN. 

The most favorable disposition of the strata actually exist- 
ing- in Alabama, as has been said above, is found in the Coastal 
Plain region, which is underlain by the sediments of the Cre- 
taceous and Tertiary formations, consisting of beds of sand, 
clay, and limestone, and others of intermediate character in 
many alternations. These lie in great sheets thinning out land- 
ward and increasing in thickness toward the Gulf, thus making 
a great flat wedge resting on the Gulfward sloping floor of the 
older rocks.* 



The ground surface in the Coastal Plain sinks from an alti- 
tude of about 600 feet near the landward margin to the level 
of the sea in the two coast counties though there are places in 
Baldwin County where the land has an altitude of fifty feet 
or more on the very border of Perdido Bay, and high land, 
100 feet and more in altitude, exists in both Mobile and Bald- 
win a few miles from the Gulf. 

The strata themselves have also a general dip or incline to- 
ward the Gulf, but at a more rapid rate than that of the land 
surface, this dip being from 25 to 40 feet to the mile, and aver- 
aging perhaps 30 feet. The conditions are thus afforded for 

*Very few of the artesian borings in Alabama have gone down 
to this floor, except in the immediate vicinity of the surface out- 
crops of the older formations. The borings at Tuskegee have pene- 
trated the granitic rocks underlying that section; and at Tuscaloosa, 
borings within a distance of one or two miles south of the last 
appearance of the rocks of the Coal Measures in the bed of the river 
at the bridge, have reached these rocks and penetrated them to con- 
siderable depths; but beyond that distance none has gone through 
the strata of the Cretaceous which here overlie the Ccal Measures. 



62 ARTESIAN WELLS. 

many artesian systems. The low relief of the country makes 
impossible, however, the great hydrostatic pressure observed 
in the mountainous regions. 

All this may be made clear by the accompanying diagram, 
taken with slight modification from Darton's Report on Arte- 
sian Well Prospects in the Atlantic Coastal Plain,* to which 
paper I am indebted for many valuable suggestions. 




Fig. 21. Section from north to south across the Alabama Coastal 
Plain illustrating its artesian conditions. 

DECLINE OR FAILURE OF ARTESIAN WELLS. 

The causes of decline in the flow of artesian wells and their 
detection, have been fully discussed in the article of Prof. 
Chamberlin, which those interested in the subject should con- 
sult. In this report we can make only brief mention of some 
of the most obvious of these. 

Increase of leakage is responsible for most of this trouble, 
and is likely to occur when the well is not piped its whole 1 
depth and especially when the boring is through limestone, the 
capillary passages and cracks in which may be gradually en- 
larged by solution, thus allowing the water to escape. 

Iron rusts quickly, especially if there are corrosive ingredi- 
ents in the water, and the piping thus rendered defective may 
cause much loss from leakage. 

Closure of the bore. — Soft and plastic beds like those of 
clay and shale, and loose ones like those of sand where the pres- 
sure is great, may yield and tend to close the bore. Or the wa- 
ter-bearing rock in the immediate vicinity of the well may be- 
come clogged by the deposition of fine silt in its pores, or by 
some form of organic life, or by a deposit of iron. 

Decline from exhaustion. — If there is but a limited accumu- 
lation of water in the distant elevated edge of the porous bed 

*Bulletin No. 138, U. S. Geol. Survey, p. 18. 



CHARACTER OF THE WATER. 63 

and it is not promptly renewed from the surface, the well may 
gradually draw it off. A decreasing flow from this cause will 
fluctuate with the rainfall and will renew itself with returning 
wet seasons. But too heavy drafts on the capacity of the water- 
hearing stratum by increase in the number of wells will be sure 
to cause a gradual failure of the artesian basin, for while the 
water supply is' constantly renewed it may easily happen that 
the drains upon the basin may be greater than the supply. Of 
all causes of decline this is probably the most common. The ob- 
vious remedy would be the attaching of spigots or the reduc- 
tion of the outlets, by which too great waste would be pre- 
vented. 

CHARACTER OF THE WATER. 

Temperature. — It is a fact derived from observation that 
below the depth at which the daily and yearly fluctuations of 
temperature are felt, the temperature of the earth increases 
with the depth at a rate which varies with the different mate- 
rials' encountered, but which may be put at an average of one 
degree of Fahrenheit for every fifty feet of descent. In our 
latitude the depth of the level of invariable temperature as it 
has been called, is roughly speaking about ioo feet. Below 
this, the increase of heat with the descent should be felt. 
Waters coming from great depths would thus be expected to 
have a higher temperature than those which have a more su- 
perficial origin, and many tests of temperature have shown this 
to be the case. The first attempt to prove this' by the records 
of Alabama artesian wells, was made by Dr. Alexander Win- 
chell in 1856, while he was in charge of a school near Eutaw. 
The results of Dr. Winchell's tests were published by him in 
the Proceedings of the American Association for the Advance- 
ment of Science, for the year 1856. The temperatures given 
vary from 64 degrees to 77.5 degrees, and the depths of the 
wells from 90 to 728 feet. The mean annual temperature of 
that part of the state (temperature of the invariable stratum) 
is not far from 64 degrees. 

After rejecting a number of observations which were obvi- 
ously erroneous, the average shown by the records was an in- 
crease of 1 degree for every 44.96 feet. 



64 ARTESIAN WELLS. 

It is obvious that artesian wells do not afford the best means 
for establishing this rate of increase, for the reason that in them 
the water almost always comes from several horizons and thus 
the temperature of the flow is likely to be lower than that of 
the deepest source. Still, it is very evident that the temperature 
of the water increases with the depth of the well, though the 
rate of this increase cannot be established by observations of 
the temperature, except in such cases where it is certain that 
the water comes from only one horizon. 

Mineral Ingredients. — Water which has long remained in 
contact with the strata of the earth will have taken into solu- 
tion a portion of the ingredients of those strata, and the pro- 
portion of dissolved ingredients will be greater in proportion 
to the length of time of such contact and the temperature there 
prevailing. Waters which come from the greatest depths are 
therefore on both accounts' likely to be more fully saturated 
with soluble matters than those which come from shallow 
depths only. We have seen above that the movements of 
groundwaters at considerable depths must be exceedingly slow 
giving them more time to effect solution. But on the other 
hand there is a great difference in the amount of soluble mat- 
ter which different strata contain, and it might easily happen 
that the water from a well of moderate depth would come from 
a bed with a large proportion of soluble salts, while one from 
a greater 4 depth might derive its water from a stratum of 
nearly pure sand containing a minimum of such salts. It is 
thus probable that the dissolved salts: of an artesian water are 
far more dependent upon the character of the water-bearing 
beds than upon the depth and temperature. As the flow con- 
tinues', the water which formed the original reservoir with a 
maximum of dissolved salts, would gradually be drawn off 
and its place would be taken by water which had not so long 
been in contact with the rocks. A slight dimunition of the pro- 
portion of dissolved salts might therefore in time be percep- 
tible if the flow were very generous. 

Inasmuch as most of the strata of the Coastal Plain of Ala- 
.bama are marine sediments, it would naturally be inferred that 
the soluble materials enclosed in them and thus given up to 
the circulating waters, would be such as were originally held 
in solution in the sea water. The chief one of these is common 



CH \k.u;ti;k m Tin: w \ti-:r. 65 

salt or chloride of sodium, and along with it are smaller quan- 
tities of the chlorides and sulphates of potassium, magnesium, 
and calcium, hi seme of the artesian waters the carbonate? 
predominate, snch as carbonates of sodium, calcium, magne- 
sium, and potassium. These waters are, in some cases at least, 
derived from fresh water sediments. 

In the nexl Chapter are given many analyses' of the waters 
from the different parts of the state and from the different 
geological formations, which will partially illustrate this 
subject. 



CHAPTER III. 

DETAILED DESCRIPTION OF THE UNDERGROUND 
WATERS OF ALABAMA. 

APPALACHIAN DIVISION. 



Talladega Mountains and Ashland Plateau. (Igneous 
and me'famorphic rocks.) 



SURFACE FEATURES. 

In the geological sketch above it has been shown that the 
rocks underlying the Appalachian division of the State are more 
or less' crystalline in texture, and below a moderate depth usu- 
allly very densely compacted and practically impervious. Near 
the surface they are often much fractured and fissured, but the 
crevices offer very limited and uncertain channels for the trans- 
mission of ground water. Most of these rocks display at the 
surface division planes of schistosity, dipping generally toward 
the southeast, but open passages along these lines are likewise 
superficial, so that at best in the original rocks the conditions 
are wanting, or at least very unfavorable, for the storage or 
transmission of ground water. 

SHALLOW WATERS. 

By the action of atmospheric agencies the rocks throughout 
this area are more or less completely covered by a mantle of 
clayey sand, the result of their decay. In favorable locations,, 
where this residual matter is not disturbed by rains, it is 
possible to trace the progress of the decay from the structure- 
less clays through rotten slates down to the unaltered crystal- 
lime rock. In some places the decay penetrates to great depths, 
ioo feet or more. Very frequently the residual matter has been 



TALLADEGA MOUNTAIN AND ASHLAND PLATEAU. 67 

removed from the place of its origin, having slid down slopes 
and accumulated in lowlying lands, leaving the comparatively 
fresh rock hare at the summits and along the exposed cliffs. 
The surface mantle thus provided, being a mixture of clayey 
matter with fragments of quartz and other undecomposed min- 
erals', is sufficiently porous to absorb and transmit with readi- 
ness water falling upon it. The moisture is thus diffused gen- 
erally throughout the mass, descending until held in check by 
the nearly impervious undecomposed rock below. The ground 
water can therefore be utilized by means of ordinary shallow 
wells and springs, but on account of the discontinuous charac- 
ter of the surface accumulations' the supply of water is in places 
somewhat limited and liable to failure in seasons of drought. 

A good many bored wells have been sunk in this residual ma- 
terial especially in Chilton county, about Thorsby, by Mr. I. E. 
Sarber. These wells get water at depths varying from 60 to 
100 feet, in a clean yellow sand underlying a hard yellow or blue 
clay, and resting on the solid granitic rock of the country. 
Into this rock the borings have pentrated as" much as 60 feet 
without any yield of water. There is generally some rise of 
water in the wells, the usual stand being from 30 to 70 feet 
below the surface. 

MINERAL WATERS. 

The Hillabee schist is the source of a number of mineral 
springs, the most important of which are Chandler's, Chambers'; 
and Jenkins', all situated on the eastern flank of the Talladega 
Mountain range. A sample of the water from Chandler's 
Spring has been analyzed by Mr. Hodges, with the following 
results : 

Analysis of water from Chandler's spring. 

Parts per million. 

Potassium (K) 3.3 

Sodium (Na) 7.5 

Magnesium (Mg) 10 3 

Calcium (Ca) 37.7 

Iron (Pe) 4.3 

Alumina (A1 2 3 ) 4.4 

Chlorine (CI) 1.7 

Sulphuric acid (SO4) 9.5 

Carbonic acid (HCO3) 186.0 

Silica 55.1 

319. S 



68 details: Appalachian division. 

This is an alkaline-saline water which, from the relatively 
large amounts of iron and the sulphates of potassium and mag- 
nesium, should poss'ess some medicinal quality. 

The water from Chambers Springs, a few miles distant from 
Chandlers' and derived from the same source, — the Hillabee 
Schist — has somewhat similar though not identical composi- 
tion, as may be seen from the following analysis by Mr. Hodges. 

Analysis of toater Chamber's Spring. "Sulphur Spring." 



Parts per million. 

Potassium (K) .3 

Sodium (Na) 5.5 

Magnesium (Mg) 19.2 

Calcium (Ca) 39.0 

Iron and Alumina (Fe 2 03,Alo0 3 ) 3.3 

Chlorine (CI) 3.0 

Sulphuric acid (SOt) ' 5.4 

Carbonic acid (HCO s ) 217.8 

Silica (SiO a ) 56.7 

350.2 



ARTF,SIAN PROSPECTS. 

In the surface beds of residual soils and other products of 
decomposition the conditions are unfavorable to the success of 
artesian borings, since these beds' are not continuous over large 
areas and are lacking in alternations of pervious and imper- 
vious strata with gentle inclination. In the underlying solid 
rocks the conditions for artesian water can not be said to be 
much more favorable, for while these rocks attain, especially 
near the surface, s'ome degree of permeability by reason of the 
joints and fissures by which they are traversed, these channels 
are not likely to be continuous for any great distance nor to 
be present at any great depth ; moreover, their position can not 
be determined beforehand and there is no certainty about strik- 
ing them. Almost any boring into these rocks will directly fill 
with water, but only under favorable local conditions is' the 
amount likelv to be sufficient to meet verv large demands. 



TALLADEGA MOUNTAIN AND ASHLAND PLATEAU. 



G9 



The manner in which the joints ma) serve as waterways for 
artesian supply is illustrated by the accompanying figure after 
M. L. Fuller.* 




Fig. 22. Well in jointed rock. 

The figure will also show how it is possible for polluted water 
to pass along these joints into the well. 

On general principles then, the area of the igneous and meta- 
morphic rocks may be considered as unfavorable for artesian 
water prospects, and experience in many States bears this out. 
On the other hand by increasing the number of borings within 
a limited space, it is often possible to obtain an adequate sup- 
ply. This has been demonstrated at Lanett in Chambers county. 
Recent studies' have also thrown some light on the artesian con- 
ditions of the crystalline rocks, and Mr. Fullerf expresses the 
opinion that it is possible by means of careful examination to 
determine in advance the probabilities of the success of a well 
within a margin of anly a few per cent, of error. 

The number of well records from this section of the Appa- 
lachian Division, is at present quite small, but the use of the 
drill is steadily increasing". 



♦Water Supply Paper No. 114, U. S. Geol. Survey, page 28. 
fEconomic Geology, Vcl. I. page 567. 



70 details: Appalachian division. 

LANETT WELLS. 

In 1S97 and '98 eight wells were bored for the Lanett Bleachery and 
Dye Works at Lanett in Chambers County. The first well as 93 feet deep 
through soil and loose rock only. It yielded thirty-six gallons per minute. 

Well No. 2 was bored 248 feet, 113 feet through solid rock which is of 
granite. This well yields 29 gallons. 

Well No. 3, is 467 feet deep, 390 feet being in solid rock; yield 62 gal- 
lons per minute. 

Well No. 4, 703 feet deep, 610 in solid rock; yield 62 gallons per minute. 

Well No. 5, 460 feet deep, 390 feet through rock; yield 17 gallons per 
minute. 
' Well No. 6, record similar to that of No. 5. 

Well No. 7, 690 feet deep, 500 feet in solid rock. Original yield about 
90 gallons per minute. 

Well No. 8, 1064 feet deep, 984 through rock; yield only 30 gallons. 

These wells are in an area of 350 or 450 feet radius. The 
rock, as above stated, is' a blue granite with seams or veins of 
flint rock, and from this flint rock comes all the water obtained 
from the wells. In boring the eighth well, the water from the 
two nearest wells was reduced, from which it has' been inferred 
that the group of wells takes up practically all the water avail- 
able within the area. The piping down to solid rock was all 
six inches in diameter. The water is considered very pure. It 
contains a trace of magnesia, and, with the exception of the 
water from the surface well, appears to* be free from lime. 
Information concerning these wells is furnished by Mr. L. La- 
nier, President of the Lanett Cotton Mills. 

ALEXANDER CITY WELLS. 

Well No. 1, depth, 525 feet; depth to water, 250 feet; diameter, 10 inches; 
depth of casing 60 feet, to rock: height of water, 17 feet; wields, 45 gal- 
lons per minute; after lowering the sand to 100 feet there was no further 
change by pumping; use, for fire purposes only; method of pumping, air 
compressor; total solids, 415.94 parts per million; volatile and organic 
matter, 112.98 parts per million; temporary hardness 46.22 parts per mil- 
lion; permanent hardness, 179.76 parts per million; mineral constituents, 
chlorine, lime, and magnesia relatively abundant, sulphuric acid, iron, 
and alumina in small amount. 

Well No. 2, depth, 350 feet; depth to water, 250 feet; diameter, 10 
inches; depth of casing 60 feet, to rock; yield, 60 gallons per minute; 
height of water, 17 feet; stand has not been lowered by pumping below 
100 feet; total solids, 461.7 parts per million; volatile and organic matter, 
51.3 parts per million; temporary hardness, 47.93 parts per million; per- 
manent hardness, 172. S9 parts per million; mineral constituents, chlorine, 
lime, and magnesia relatively abundant, sulphuric acid, iron, and alumina 
In small amount. 

The composition of the water from the two wells appeared to be 
■substantially the same. 



\IT AI.AC1LIAX VALLEYS. 71 

AUBURN, LEE COUNTY. 

A well was bored at Auburn in 1899 by M. L. Fullan, the 
details of which will be found in the description of Lee Count\ 
in the Coastal Plain division below. 

A ppalachian Valleys. 

SURFACE FEATURES. 

The geological formations occurring in the Appalachian vai- 
leys range from Cambrian up to Lower Carboniferous inclu- 
sive. The prevailing rocks are limestones and dolomites, but 
along with them are subordinate beds of shale, sandstone, and 
conglomerate. 

The great limestone formation is the Knox dolomite, which 
occupies a. very large proportion of the entire area. Of less 
importance are the Trenton and Tuscumbia (Lower Carbon- 
iferous) limestones, which usually outcrop only along the mar- 
gins of the valleys or the bases of the bordering hills. 

In the lower part of the Cambrian occur the most important 
bodies of shale, which underlie large areas' in the Coosa Valley 
and smaller ones in the central parts of the lesser valleys. Other 
• bodies of shale inclosing beds of sandstone, occur among the 
strata of Clinton (Red Mountain) ridges. Still other shales 
make a large part of the area of the Lower Carboniferous 1 along 
the western border of the Coosa Valley. 

The sandstones are fairly well distributed among the various 
formations, but the greatest bodies, including conglomerates, 
are found in the Coosa Valley, where they rise into veritable 
mountains. The sandstones of the Clinton (Red Mountain) 
ridges and of the Lower Carboniferous' formations may under 
certain conditions be of importance in connection with artesian 
prospects, which are considered below. 

SHALLOW WATERS. 

While the rocks of this subdivision are not as a rule char- 
acterized by any serviceable degree of porosity, as will be seen 
later, yet they are all covered more or less completely by soils' 
and other residual matters resulting from their decav and 



72 DETAILS : APPALACHIAN DIVISION. 

weathering, and these surface accumulations are fairly well 
adapted to 1 the absorption and storage of the rainfall, so that 
springs and open wells are common throughout this area ex- 
cept where it is too thoroughly underdrained by cavernous lime- 
stones. As is the case, however, with all residual accumula- 
tions, these surface beds are not commonly in continuous bo- 
dies of great extent and thus their water supply is more or less 
closely dependent on local rainfall. 

Of much greater importance in this connection are the great 
limestone springs, or "big springs," especially of the Knox 
dolomite and in less degree of the Tuscumbia (Lower Carbon- 
iferous) limestones. Both these limestones, in some parts', are 
highly siliceous or cherty, and like all limestones are traversed 
near the surface by fissures, channels, and caverns', formed or 
enlarged by the solvent action of the circulating waters, which 
also, dissolving the purer parts of the limestone, leave behind 
the chert in great open masses of the highest degree of per- 
meability. In consequence of thes'e conditions much of the 
rainfall in these terranes finds it way sooner or later into these 
subterranean channels forming streams which emerge as "big 
springs." 

It need hardly be said that wells or borings may sometimes' 
hapren to be sunk on one of these underground streams, from 
which large supplies of water may be obtained by pumping,* 
though in the nature of things the water is not likely to rise in 
the wells, having free outlet through the underground chan- 
nel. In Birmingham, and probably in many other places, such 
streams have been utilized by air-lift appliances. 

It would be hardly possible to enumerate all the great lime- 
stone springs of this section, but the following are well known ; 
In the Coosa Valley, the springs about Piedmont, Alexandria, 
Jacksonville, Coldwater Spring near Anniston, Oxford, Tal- 
ladega town, Kelley's above Talladega, Fayetteville, Monte- 
vallo, etc. ; in the lesser valleys, Village Springs, Springville, 
Hawkins, Elyton, Bessemer, or Jonesboro, Bucksville, Tanne- 
hill, Roup's, Guntersville. 

MINERAL WATERS. 

The mineral waters of the Appalachian valleys show a great 
variety in their composition on account of the variety of mate- 



APPALACHIAN VALLEYS. 73 

rials making up the formations in which they are found. The 
most prolific sources of these mineral waters are, perhaps, the 
ferruginous, calcareous' shales of the Cambrian, and the black 
bituminous shales of the Devonian and Lower Carboniferous; 
and the most common mineral waters from these formations 
are sulphur and chalybeate waters, usually more or less cl»sely 
associated, making classification rather difficult. 

Sulphur and Chalybeate Waters, 
jones springs. 

Seven miles' southwest of Gadsden on the Ashville road, in 
the N. E. quarter, N. E. quarter, Section I, Township 13. 
Range 5 F,.. is a white sulphur spring - on the place of Mr. Jones. 
The spring flows daily from 800 to 1000 gallons and the water 
is very agreeable to the taste. On the same land there is a 
large spring coming out of the limestone formation. 

ST. CLAIR SPRINGS. 

Farther southwest in Section 3, Township 15, Range 2 E., 
are the St. Clair Sulphur Springs. The waters come from the 
limestones overlying thin-bedded calcerous shales of the "Flat- 
woods." They are pleasant to the taste and not too strongly 
impregnated with sulphur. Ample accommodations are pro- 
vided for visitors. 

There are six springs along a brook running a little east of north. 
The first five in order of occurrence from the south, are (1) Black Sul- 
phur, (2) Sulphur. (3) Freestone, (4) White Sulphur, and (5) Red Sulphur. 
No. 6, a short distance west of No. 5 is known as Lithia Spring. Nos. 1 
and 2 are considerably stronger in sulphur than either No. 4 or No. 5. 
but in other respects are similar. All the sulphur waters contain lithium 
and traces of barium and strontium. No lithium could be detected in 
No. 6, which is also free from barium and strontium. The temperatures 
of the waters were, No. 4, 06.5°; No. 5, 63.5°; and No. 6,(J0.5°, the tem- 
perature of the air at the same time being 73.8°. 



74 DETAILS : APPALACHIAN DIVISION. 

Analysis of water from* springs No. 4, 5 and 6, St. Glair. 



Parts per million. 

No. 4 No. 5 No. 6 

Potassium (K) 1.2 1.8 .6 

Sodium (Na) 8.3 23.6 3.5 

Lithium (Li) ' trace, stg. trace, none 

Magnesium (Mg) 16.4 14.8 17.3 

Calcium (Ca) 36.9 31.8 37.5 

Barium (Ba) trace, trace. 

Strontium (Sr) trace, trace. 

Iron and alumina (Fe 2 O s , A1 2 3 ) 2.2 2.2 1.3 

Chlorine (CI) 4.9 11.5 4.1 

Sulphuric acid (S0 4 ) 4.8 

Carbonic acid (HCO3) 209.1 170.0 161.2 

Sulphuretted hydrogen (H 2 S) .3 8.2 

Silica (Si0 2 ) 13.3 16.9 18.4 

292.6 280.8 248.7 



No. 4 "White sulphur." 
No. 5 "Red Sulphur." 
No. 6 "Lithia." 

TALLADEGA SPRINGS. 

Both sulphur and chalybeate waters are found at Talla- 
dega Springs, Plate III, but their origin is difficult to determine 
with certainty, since the springs arise from the limestones at 
the foot of mountains of the Weisner quartzite (Cambrian). 
Inasmuch as these mountains are mostly in contact with much 
younger strata on tne north by reason of faulting, it is prob- 
able that the springs have their origin in the Devonian or 
Lower Carboniferous black shales, both of which appear in the 
near vicinity, though the rock from which the water issues 
seems to be the Pelham limestone. There are many conven- 
iences for visitors here and the waters are well known. 



Below is an analysis of this water by Prof. W. C. Stubbs 
taken from Bulletin 32, U. S. G. S. 1886 but recomputed to 
ionic form and parts per million by Mr. Hodges. 

Determinations by Mr. Hodges of the sulphuretted hydrogen 
of this water in 1904 and 1905 gave only about 19 parts per 
million. 



APPALACHIAN VALLEYS. 75 

Analysis of water from Talladega Springs. 



Parts per million. 

Potassium (K) 77.4 

Sodium (Na) 127.7 

Magnesium (Mg) 4.C 

Calcium (Ca) 115.3 

Alumina (A1 2 3 ) 24.8 

[ron (Fe) trace 

Chlorine (CD 55.5 

Sulphuric acid (S0 4 ) 131.7 

Carbonic acid <HC0 3 ) 368.0 

Sulphuretted hydrogen (H 2 S) 539.2 

Silica (SiO a ) 42.5 

I !m;.t 



SHELBY STRINGS. 

Shelby Springs, in Section 14, Township 21, Range 1 W., 
(Plate IV) comprising two sulphur springs with white deposits, 
a chalybeate spring, and a magnesium spring, come from the 
black shale of the Subcarboniferous. which here underlies so 
much territory. In the near vicinity is a large limestone 
spring. 

The composition of one of the sulphur waters of Shelby 
Springs', viz., that from a spring near the pavilion shown in 
Plate IV, is given in the following analysis by Mr. Hodges. 

Analysis of water from Shelby Springs, ''White Sulphur." 



Parts per i 

Potassium (K) 1.2 

Sodium (Na) 7.3 

Magnesium (Mg) 7.9 

Calcium (Ca) 47.8 

Iron and Alumina (Feo0 3 ,Alo0 3 ) 1.3 

Chlorine (CI) 2.4 

Sulphuric acid (S0 4 ) 9.6 

Carbonic acid (HCO s ) 80.1 

Sulphuretted hydrogen 'BUS) .8 

Silica (SiO») 3.6.4 



194.8 



HAWKINS WELL. LEEDS MINERAL WATER. 

This well is near the line of the Southern Railway, in Jef- 
ferson County a mile or two east of Leeds, (Plate V). The 



76 DETAILS : APPALACHIAN DIVISION. 

well is near the boundary of St. Clair County, and is an ordi- 
nary open well about 50 feet deep. The composition of the 
water is shown in the accompanying analysis, by Mr. Hodges. 

Analysis of Leeds Mineral Water ; Hawkins Well. 



Parts per million. 

Potassium (K) ' 6.7 

Sodium (Na) 20.5 

Magnesium (Mg-) .9 

Calcium (Ca) 2.5 

Iron (Fe) ' 2.1 

Aluminum (Al) 4.6 

Chlorine (CI) 20.5 

Sulphuric acid (S0 4 ) 35.2 

Carbonic acid (HC0 3 ) 34.5 

Silica (SiQ 2 ) 19.9 



147.4 



The well is in Subcarboniferous' starta at the eastern foot ot 
Little Oak Mountain, in the Cahaba Valley. This water is 
bottled and has an extensive sale in the State. 

ALABAMA WHITE SULPHUR SPRINGS. 

These springs are in the southwest corner of Section io, 
Township 4, Range io E., in Wills Valley, Dekalb County. 
The surface rocks at the springs are the cherty limestones of 
the Subcarboniferous', but the underlying Devonian shale is 
undoubtedly the source of the sulphur water. This black shale 
is rich in iron pryrites and its decomposition produces the sul- 
phur. There are here five springs (Plate VI), three of which 
are more or less impregnated with sulphur, though none of 
them very strongly. 



GEOLOGICAL SURVEY OF ALABAMA. UNDERGROUND WATER RESOURCES. PLATE V. 




Hawkins Well. (Leeds Mineral water). Jefferson County. 



APPALACHIAN VALLEYS. 77 

Mr. Hodges has analyzed the waters from two of the springs, 
viz, the White Sulphur and the Freestone, with the results given 
below : 

Analyses of water from Alabama White Sulphur Springs. 



Parts per million. 

No. 1 No. 2 

Potassium (K) 3.2 trace. 

Sodium (Na) 15.7 1.8 

Lithium (Li) trace. 

Magnesium (Mg) 55.8 5.3 

Calcium (Ca) 118.3 74.6 

Iron (Fe) ' .7 .6 

Alumina (Al 2 O s ) 1.3 2.1 

Chlorine (CI) 4.2 1.4 

Sulphuric acid (S0 4 ) 304.2 10.5 

Carbonic acid (HC0 3 ) 294.5 246.2 

Sulphuretted hydrogen (H 2 S) 8.1 

Silica (SiO a ) 25.8 11.0 

S31.8 353.5 



No. I "White sulphur." 
No. 2 "Freestone."' 

The Plate (VI) shows the White Sulphur Spring - , No. I, in 
the foreground, and the Freestone Spring, No. 2, in the back- 
Ground. 



BLOUNT SPRINGS AND VICINITY. 

The most noted sulphur springs in the State are the Blount 
Springs, situated near the end of Sequatchee (Browns) Val- 
ley, in the southwest quarter of Section 6, Township 13, Range 
2 W. 

The plate, No. VII, shows the pavilion at Blount and the 
positions of the several springs mentioned below ; while the 
diagram, figure 23. will make these positions more definite, and 
will serve for their better identification. 

The little marble basins in front of the pavilion mark the 
places of most of the springs. 



78 



DETAILS : APPALACHIAN DIVISION. 




Fig. 23. Diagram of Blount Springs. 



Quantitative analyses of the water of three of these springs 
have been made by Mr. Hodges, and qualitative examinations 
of three others', with the results given below. 

Analyses of Blount Springs Sulphur Waters. 



Parts 
No. 1 

Potassium (K) 14.2 

Sodium (Na) 234.3 

Lithium (Li) 1.2 

Magnesium (Mg) 24.3 

Calcium (Ca) 51.4 

Barium (Ba) 4.6 

Strontium (Sr) 2.4 

Iron (Fe) .8 

Alumina (Al 2 O s ) 15 

Chlorine (CI) 325.1 

Bromine (Br) 1.9 

Iodine (I) trace. 

Sulphuric Acid (S0 4 ) trace. 

Carbonic acid (HCO s ) 279.1 

Sulphuretted hydrogen (H 2 S) 56.5 

Silica (Si0 2 ) 26.5 

1023. S 
*Present taut not determined. 



per million. 


No. 2 


No. 3 


18.8 


11.8 


232.0 


217.8 


* 


* 


24.9 


23.1 


53.2 


50.6 


* 


* 


* 


* 


1.0 


.8 


1.5 


1.3 


320.1 


297.3 


* 


* 


trace. 


trace. 


trace. 


trace. 


276.2 


257.3 


54.2 


53.1 


19.7 


16.6 



996.6 



92S.9 



APPALACHIAN VALLEYS. 79 

A qualitative test of springs No. 5 and G showed them to be very Imilar 
to No. 1. A qualitative examination of spring No. i gives of solid dis- 
solved matter 555.75 parts per million. The wati ilphuretted and 

contains sum.' sulphates; lithium is also present. 

The temperature was found to be practically the same in all these 
springs, t;3.5° F., the temperature oi the air at the same time being 82° F. 
A\"ith the exception of No. 4 they were all strongly sulp They 

furnish an abundant supply of water for drinking and baths, No. 1, the 
largest, having a flow of about 3 gallons per minute. 

The presence of some constituents in relatively Large quanti- 
ties, not commonly found in Alabama mineral waters, makes 
these springs noteworthy. They contain more sulphuretted hy- 
drogen and lithium than any other water in the State of whichh 
a record is available, the presence of the latter being easily 
detected with the spectroscope in the water as taken from the 
spring, without any concentration. Salts of barium and stron- 
tium are also present. 

Cold Spring. — This is a good type of the "Big" springs 
so characteristic of the Lower Carboniferous rocks, and would 
not properly be considered as a mineral spring. It is about one 
mile south of Blount Springs Hotel near the bank of Randolph 
Creek. The flow of water is very large. The temperature is 
59°, the temperature of the air at the same time being 

79°- 

The analysis given below T show its principal ingredient to 
be carbonate of lime. It is free from sulphuretted hydrogen 
and any large amount of sodium chloride, which are so plenti- 
ful in the Blount Springs water proper. 

Analysis of water from "Cold Spring," near Blount Springs. 



Parts per million. 

Potassium (K) 1.3 

Sodium (Na) 7.2 

Magnesium (Mg) 4.4 

Calcium (Ca) 5S.7 

Iron and Alumina (Fe 2 03.Al 2 03) 1.7 

Chlorine (CD 9.9 

Sulphuric acid (SO,) 8.9 

Carbonic acid (HC0 3 ) 194.8 

Silica (Si0 2 ) 14. S 

301.9 



Glenwood Spring. — Of somewhat similar nature is a water 
from the Oxmoor sandstone ridge, near Blount Springs, or: 



80 DETAILS : APPALACHIAN DIVISION. 

the property of Mr. G. D. Fitzhugh. This spring is' in the N. 
W. quarter, N. E. quarter, Section 6, Township 13, Range 2 W., 
and is called Glenwood Spring. 

Analysis of water from Glenwood Spring, near Blount Springs. 



Parts per million. 

Potassium (K) 1.0 

Sodium (Na) 4.5 

Magnesium (Mg) 2.1 

Calcium (Ca) 28.1 

Iron and alumina (Fe 2 3 ,Al 2 3 ) 1.1 

Chlorine (CI) 5.3 

Sulphuric acid (SO J S.4 

Carbonic acid (HCO a ) 91.8 

Silica (Si0 2 ) 12.2 

154.5 



Harrell's Well. — The following analysis by Mr. Hodges of 
the water from a well 90 feet deep on the property of Mr. W. 
F. Harrell, one mile north of Blount Springs, shows it to be 
a chalybeate water, and it is reputed to have valuable medi- 
cinal character. 

Analysis of toater from Harrell's well, near Blount Springs. 



Parts per million. 

Potassium (K) 1.0 

Sodium (Na) 6.6 

Magnesium (Mg) 7.4 

Calcium (Ca) 53.9 

Iron and alumina (Fe 2 3 ,Al 2 3 ) 12.4 

Chlorine (CI) 15.7 

Sulphuric acid (SO4) 19.3 

Carbonic acid (HC0 3 ) 167.7 

Silica (Si0 2 14.7 

298.2 



BORDEN-WHEELER SPRINGS. 



This much visited resort is on the Seaboard Air Line R. R., 
in Cleburne County, (Plate VIII.) 

The accompanying analysis of the water, by Mr. Hodges, will 
show its character. 



J *'j 


fcS ' WW >'r .;•■'' r ( 




Ha 




y|fH*-. V- * . 






_iL' *5jp«§ 




♦I 


ife. 


s « . t • 



APPAL Will w VALLEYS. 81 

Analysis of water from Borden Wheeler springs. 



Parts per million. 

Pota turn (K) .9 

Sodium (Na) 4.0 

Magnesium (Ms) 6.7 

Cal am (Ca) 36.3 

Iron (Fe) L.6 

Alumina i.mii.i .3 

1.7 

Sulphuric acid (SO,) 22.9 

tiii icid (HO » s ) 131.6 

Silica (SiOo) 19.9 

225.9 



OTHER SPRINGS. 

The Devonian black shales give rise to numerous sulphur and 
chalybeate springs in Calhoun County and elsewhere. The sul- 
phur springs in the N. W. quater, S. W. quarter. Section 30, 
Township 15, Range 6, E., in Calhoun County, occur in black 
shales interstratified with seams of resinous-looking brown and 
grayish sandstones. The water is pleasant to the taste, being 
not too strongly impregnated with sulphur. In the S. W. 
quarter, N. W. quarter, Section 30, Township 16, Range 4 E., 
in St. Clair County, a group of sulphur and chalybeate springs 
occur in the same black shales. A chalybeate spring from the 
Subcarboniferous shale is recorded in the S. E. quarter, N. W. 
quarter, Section 1, Township 15, Range 6 E., also in Calhoun 
County. 

Of chalybeate springs there is no lack in the ether formations 
in this section; thus in the Weisner (Cambrian) sandstones 
are the Chocco Springs', near Talladega, in the southeast cor- 
ner of Section 17, Township 18, Range 5 E., comprising two 
chalybeate and several freestone springs ; also another fine and 
well-known chalybeate spring in the northeast corner of Sec- 
tion 2, Township 15, Range 9 E., in Calhoun County. Chaly- 
beate waters are also abundant in the strata just under the bluff 
of the lower conglomerate of the Coal Measures capping Look- 
out and Raccoon mountains. These are noticed under "Coal 
Measures." 



82 DETAILS : APPALACHIAN DIVISION. 



INGRAM WELL. 



The Devonian black shale of Calhoun County yields another 
water of rather interesting composition from the Ingram well, 
28 feet deep, in the E. half, S. W. quarter, Section 26, Town- 
ship 14, Range 6 E., one and one-half miles east of Ohatchee. 
(Plate IX A.) The analysis below is by Dr. J. W. Mallett* 

Analysis of Ingram lithia water from well near Ohatchee. 



Part? per million. 

Sodium (Na) 6.37 

Potassium (K) 1.58 

Lithium (Li) .06 

Manganese CMn) ■ .11 

Calcium (Ca) 44.21 

Strontium (Sr) 16 

Ammonium (NH 4 ) .20 

Zinc (Zn) .29 

Iron (Fe) .70 

Maganese (Mn) .11 

Copper (Cu) .06 

Aluminum (Al) .27 

Sulphuric acid (S0 4 ) 17.13 

Chlorine (CI) '. 5.68 

Carbonic acid (HCO s ) 147.72 

Nitric acid (NO a ) .13 

Silica (Si0 2 ) 39.68 

Fluorine (F) trace. 

26S.82 



^Expressed by analyst in grains per gallon and hypothetical com- 
binations; recomputed to ionic form and parts per million at U. S. 
Geological Survey. 

Saline Waters, 
landers well and gary springs. 

Besides chalybeate waters, the variegated shales of the Cam- 
brian yield strongly saline waters of medicinal quality, as' may 
be seen from the following analyses of water from the well of 
Mr. A. M. Landers, of Jacksonville, and from the Gary 
Springs, near Centerville, both analyses of Mr. Hodges. 



GEOLOGICAL SURVEY OF ALABAMA. UNDERGROUND WATER RESOURCES. PLATE I\. 




A. Ingram Well, near Ohatchee. Calhoun County. 




B. Gate City Well, Jefferson County. 



APPALACHIAN VALLEYS. 83 

A naii/sis of water from &.. M. Landers's well, Jacksonville. 



Parts per mi 

Sodium (Na) 

Magnesium (Mg) 

Calcium (Ca) -'!:•■; 

[ron and Alumina 1 1 '• ■■•< ' .. A I ■' »s) ■'■! 

Chlorine (CI) ,,,-,'- 

Sulph I (SO*( v l\\ ■;: 

Carbonic arid (HCOs) ' 

Silica (SiO s ) da -* 

I 75$. ' 



Analysis of water from Gary Springs, near Centerville. 



Parts per million. 



Potassium (K) f"i 

Sodium (Na) JH 

Magnesium (Mg) ..;:•.' 

ium (Ca) 4d °-£ 

Iron and Alumina (Fe 2 0s,Al 2 3 ) »■» 

Chlorine (CI) -,.,.,:?,' 

Sulphuric acid (SO*) ] V:!'.> 

Carbonic acid HCO s ) *--■- 

Carbon (lh.xi.le (CO*) «./ 

Silica (SiOo) __!_! 

2091.1 
Free carbonic acid, 242 cc. per liter. 



The calcareous shales of the "Flatwoods" of Coosa River 
above Gadsden yield also mineral water of very decided char- 
acter, as may be seen from the following analysis, by Mr. 
Hodges. 

BALL FLAT WELL. 

Analysis of water from John B. Smith's toell, Ball Flat. 



Parts per million. 

Potassium (K) 5.9 

Sodium (Na) J , . 

Magnesium (Mg) •"{•» 

Calcium (Ca) /VVAV ok 

Iron and alumina (Fe 2 3 .Al 2 3 0) ••■•.' 

Chlorine (CD ,\j.'-% 

Sulphuric acid (S0 4 ) '. 

Carbonic acid (HC0 3 ) 1 - •; 

Silica (Si0 2 ) - u - u 

2181. S 



84 DETAILS : APPALACHIAN DIVISION. 

ARTESIAN PROSPECTS. 

All the older rocks which have lain below a thick covering 
of younger formations for a long time, even though originally 
porous, have had their porosity greatly diminshed by the filling 
of the pores with silt or clay, or more commonly, in the deeper 
zones, of flow, by the deposition of mineral matter. Limestones 
are, in their original condition, in most cases among the most 
compact and least porous of rocks ; shales, while possessing a 
high degree of porosity, are yet almost impermeable by reason 
of the small size of the pores and the great friction encounter- 
ed by the water in passing through ; sandstones have originally 
the greatest degree of permeability, by virtue of the compara- 
tively large size of the individual grains, and consequently of 
the pores between them. The sandstones of the Appalachian 
valleys, having remained long deeply buried, have lost a part 
of their porosity as above explained, so that in general all the 
rocks underlying this area must be considered as poorly adapted 
to the absorption and transmission of water. 

On the other hand, the limestones may be open textured from 
several causes. Near the surface, as above shown, they may be 
jointed and fissured and these openings' may be enlarged by 
solution in circulating waters ; in the alteration of limestone into 
dolomite there is a diminution in the volume of the rock and 
a consequent development of shrinkage cracks ; where siliceous 
or cherty limestones have been exposed at the surface for a 
long time the lime may be leached out and the chert left as an 
exceedingly open and porous mas's through which the waters 
may pass without obstruction. Some of the sandstones still 
possess a reasonable degree of porosity. The shales are al- 
ways good covers and underlying beds' for the porous strata, 
and in many places the alternations of pervious and impervious 
beds at a gentle inclination fulfil some of the requisites of 
an artesian system, so that under favorable local conditions 
artesian water may be found in much of this area. These fa- 
vorable conditions may be offset, however, in several ways. 
The fissures are likely to be narrowed or even closed at con- 
siderable depths, and they are rarely continuous for any great 
distance ; the same may be said of the openness' of texture pro- 
duced by other causes. Moreover, the geologic structure may 
give rise to still other opposing conditions. As already stated, 



APPALACHIAN VALLEYS. 85 

the rocks in all those valleys have been benl upward into anti- 
clinal arches which are often lapped over to one side; or several 
folds may he compressed together, and there may be further 
complications by faulting. These disturbances are more in the 
eastern part of this area than farther west. As a consequence 
the strata, even when other conditions are favorable, may stand 
at too steep an inclination to be well adapted to artesian bor- 
ings, for the water in the porous bed would be carried beyond 
available depths too quickly. 

The horizons which have yielded artesian water, so far as 
the collected records go, are the lower Cambrian limestones 
and sandstones about Anniston and the Lower Carboniferous" 
strata of Red Mountain, near Birmingham. 

The Weisner sandstone is a great mountain-making forma- 
tion running with occasional breaks from the Georgia line 
southwestward by Piedmont, Jacksonville, Anniston, and Tal- 
ladega to the Kahatchee Hills near Talladega Springs. The 
foothills of this ridge are covered with a thick layer of residual 
deposits resting on the other Cambrian formations. 

ANNISTON. 

Several borings have been made at Anniston with the re- 
sults, given below. These borings pass through the residual 
matter near the surface and the limestones into a sandstone in 
which the w r ater is obtained. This may be the Weisner sand- 
stone, but reliable identifications have not been made. 

Well No. 1. Charcoal Furnace; diameter, 8 inches; d£pth, 260 feet; 
water rises within 4 feet of the surface; capacity not determined, but 
seems to have been several gallons per minute; well was abandoned be- 
cause of the loss of tools. 

Well No. 2, Charcoal Furnace; drilled in 1886 by Charles Morgan; diam- 
eter, 6 5-8 inches; depth, 558 feet; water at 550 feet, rising to within 
4 feet of the surface. The boring struck decomposed Cambrian lime- 
stone at 32 feet, in which it continued all the way, except for 
8 feet of porous sandstone at the bottom. The well is located 
about 40 feet from No. 1, on ground about 30 feet lower than the water- 
works well. The limestone is thicker at the furnaces. While drilling in 
the limestone the water level in No. 1 was affected, but on completion 
the limestone was cased off. A pump delivering a solid 5-inch stream did 
not diminish the supply after a twenty-four hour test. 

Coke Furnace well; drilled in 1899; diameter, 10 inches; depth, 480 feet; 
height of water, SO feet. The well was begun at the bottom of a shaft 
which was sunk 126 feet through yellow clay, 10 feet through shale, and 
344 feet into limestone. The flow of water into the shaft from the well 



86 DETAILS I APPALACHIAN DIVISION. 

was determined by measurement to vary from 1,200 to 1,900 gallons per 
minute. When drawing- 1,800 gallons per minute the pumps held the level 
constantly at 5 feet below the bottom of the shaft. 

City water-works well, diameter, 8 inches; depth, 310 feet; depth to 
water, 280 to 310 feet; water rises to within 30 feet of the surface; capacity 
under pump, 1,000 gallons per minute without lowering; quality, good; 
temperature 60 degrees. The well is supposed to be entirely in Cambrian 
rocks. It was started at the bottom of a shaft 120 feet deep. From the 
surface the materials were: Soil, a few inches; yellow clay, 4 feet; coarse 
gravel, 36 feet; limestone, somewhat decomposed and interspersed with 
numerous seams and jointed masses, 240 feet; flint, 2 inches; sandstone, 
at first coarse grained, but becoming gradually porous, 30 feet. 

In the upper part of the Lower Carboniferous beds, equiva- 
lent in general to the Bangor (Chester or Mountain) • lime- 
stone division of geologists, are some thick bodies of shales and 
sandstone which have received the name Oxmoor, from their 
great development at the village of that name in Shades Val- 
ley. The same strata reappear prominently east of the Coosa 
coal field and between that field and the great Coosa Valley. 
Some of these sandstones are quite opentextured and free from 
lime, and thus well fitted for the absorption and transmission of 
water. In many places they have a gentle slope to the south- 
east, and being inclosed between shales form good artesian res- 
ervoirs. 

GATE CITY. 

Records have been collected of artesian wells in these strata 
at only one place, viz, the eastern slope of Red Mountain near 
Gate City, Birmingham, yet on general principles there should 
be reasonable expectation of success in borings at other points 
in Shades Valley, as well as in the region between the Coosa 
coal field and Coosa Valley. 

Borings made by Mr. DeBardeleben in Shades Valley south 
and southwest of Birmingham, in prospecting for the Red 
Mountain ore seam, have recently fully realized this' expecta- 
tion. 

The Gate City wells are in the S. E. quarter, N. W. quarter, 
Section 26, Township 17, Range 2 W., in Shades Valley, at 
the base of the Red Mountain ridge. Here were formerly two 
large limestone springs about 30 feet apart. Four wells have 
been bored within a radius of 100 feet of these springs; two 
of them are 10 inches in diameter, the other two 6 inches. The 



APPALACHIAN VALLEYS. 87 

water in all the wells stands at about the height of the two 
springs mentioned, and overflows or stands a few feet below the 
surface according to the elevation of the mouth of the well. 
The borings are 25,85,103, and 344 feet deep respectively. The 
sinking- of these wells has diminished the flow of one of the 
springs, but the other does not seem to be affected. One of 
these wells is shown in Plate IX. B. 

Tn the N. W. quarter of the S. E. quarter of Section 26, 
Township 17, Range 2 W., and a short distance southeast of 
the springs and wells just mentioned are other springs. The 
water from one of these — E, T. Cox's — has been analyzed by 
Mr. Hodges with the following results. 

Analysis of water from E. T. Cox's spring, Shades Valley. 



Parts per million. 

Potassium (K) .8 

Sodium (Na) : 8.2 

Magnesium (Mg) 5.6 

Calcium (Ca) 22.8 

Iron and Alumina (Fe»0 3 .Al 2 3 ) 3.2 

Chlorine (CI) 3.3 

Sulphuric acid (So 4 ) 6.6 

Carbonic tcid (HCO.,) 106.6 

Silica (Si0 2 ) 43.3 

200.4 



The sandstones of the Clinton (Upper Silurian) formation 
might locally furnish an artesian supply, but as they are gen- 
erally calcareous they probably have low porosity. Their posi- 
tion, however, between impervious shales, is favorable. 

In the lesser valleys and the two Red Mountain ridges (east 
and west) the great preponderance of limestones and calca- 
reous shales among the strata and above all their high angle of 
dip are unfavorable for artesian prospects, though, as above 
mentioned favorable for "big springs." 



88 details : appalachian division. 

Coal Measures (Carboniferous Rocks) 

The strata of the Coal Measures consist in the main of the 
sandstones, conglomerates', and shales ; the coal seams form a 
very small percentage of the entire thickness and there are a 
few thin beds of impure limestone. 

shallow waters. 

In consequence of weathering these rocks are covered with 
a mantle of residual material — sands, clays, and loams of vary- 
ing thickness' according to the locality ; though in some places 
this mantle has been entirely removed by erosion leaving bare 
rocks at the surface. Springs and open wells are everywhere 
sources of water for domestic use, but on account of the non- 
continuity of these surface beds and their variable thickness 
the supply is intimately dependent on occasional conditions, and 
is prone to diminish or- fail in times of long-continued drought. 
These springs' escape usually just above a bed of shale or a 
coal seam. The latter is an especially effectual hindrance to 
downward percolation, and in consequence wet, fern-covered 
benches along the hillsides' and in the ravine heads are con- 
sidered good guides in prospecting for coal. 

The sandstone strata near the base of these measures are gen- 
erally good collectors and storers of surface waters, especially 
near the cliffs' and escarpments overlooking the valleys. The 
springs at Mentone, on Lookout Mountain; on Monte Sano, 
near Huntsville ; and on Shades Mountain, near Oxmoo<r, are 
instances. The waters from Towne's spring and the De Soto 
Springs on Shades Mountain have been found by analysis (see 
below) to be alkaline-carbonate waters, with, however, no ex- 
cessive amount of dissolved mineral matter. 

Toward their southwestern limit the Coal Measures are 
covered in part by later formations; — the Tuscaloosa and La- 
fayette — and as these consist in the main of unconsolidated 
sands and pebbles, the surface-water supply dependent upon 
them is much more reliable and usually never failing. 

MINERAL WATERS. 

While the Coal Measures are prolific in mineral waters, main- 
ly sulphur and chalybeate, there are comparatively few places 



GEOLOGICAL .SURVEY OF ALABAMA. UNDERGROUND WATER RESOURCES. PLATE X. 




A. Cook Springs, St. Clair County. 






B. Mentone Spring, Dekalb County. 



COAL. MEASURES. 89 

where they have been utilized and where accommodations have 
hern provided for visitors. 

COOK SPRINGS. 

These springs. (Plate X. A), located on the Seaboard Air 
Line, in the Coosa coal field, are well situated and improved. 
There are several springs of different kinds, among them a 
chalybeate and a sulphur spring. With the exception of these 
two which have respectively 269.8 and 274.1 parts per million, 
the waters contain comparatively little dissolved mineral waters, 
as may be seen by the subjoined analyses by Mr. Hodge: 

Analyses of icater from Cook Springs. 



Parts per million. 
No. 1 

Sodium (Na) 30.2 

Potassium (K) 2.6 

Magnesium (Mg) 4.1 

Calcium (Ca) 22.6 

Iron and alumina (Fe20 3) Al 2 03) 22.6 

Chlorine (CI) 5.3 

Sulphuric acid (S0 4 ) 5.3 

Bicarbonic acid (HCO3) 157.1 

Sulphuretted hvdrogen (HoS) .4 

Silica (Si0 2 ) 43.8 

Total 274.1 94.7 269.8 40.5 



No. 2 


No. 3 N( 


6.9 


11.0 


3.7 


1.5 


3.7 


.9 


1.3 


2.6 


1.0 


10.0 


117.2 


2.8 


4.0 


10.8 


.8 


5.3 


3.5 


3.5 


7.9 


2.1 


2.1 


38.3 


74.1 


14.9 


19.5 


44.8 


10.8 



No. 1 "Sulphur spring." 
No. 2 "Lithia or Magnesia."' 
No. 3 "Chalybeate." 
No. 4 "Lithia." 



SPRINGS OX SHADES MOUNTAIN. 



At and near the summits of the high plateaus of the Coal 
Measures, adjacent to and overlooking the valleys, are many 
fine springs, chiefly chalybeate, though frequentlv alkaline-car- 
bonate like the Cook Springs' just mentioned. Of this kind two 
springs on Shades Mountain, near Oxmoor, Jefferson County, 
of which analyses by Mr. Hodges are given below : 



90 DETAILS : APPALACHIAN DIVISION. 

Analysis of water from DeSoto Spring No. 1, near Oxmoor. 



Parts per million. 

Potassium (K) .6 

Sodium (Na) 7.3 

Magnesium (Mg) : ; 3.2 

Calcium (Ca) 34.1 

Iron and Alumina (Fe 2 3 ,Al 2 3 ) 5.1 

Chlorine (CI) 1.7 

Sulphuric acid (S0 4 ) 1.9 

Carbonic acid (HCO a ) 129.4 

Silica (Si0 2 ) 36.9 

220.2 



In the same vicinity is another spring - , on the property of 
Mr. John Townes, of Birmingham : 

Analysis of water from Towne's spring, near Oxmoor. 



Parts per million. 

Potassium (K) 2.3 

Sodium (Na) ' 15.8 

Magnesium (Mg) 3.9 

Calcium (Ca) 21.0 

Iron and Alumina (Fe 2 03,Al 2 03) 3.6 

Chlorine (CI) 5.3 

Sulphuric acid (S0 4 ) 5 

Carbonic acid (HCO3) 118.4 

Silica (SiO s ) 31.1 

201.9 



Another well-known spring close by is the Hale Spring. As 
a matter of fact springs of the finest chalybeate water are nu- 
merous, and one might say characteristic, in the basal con- 
glomerates and other strata of the Coal Measures wherever 
these appear in cliffs overlooking the valley. 

SPRINGS ON LOOKOUT MOUNTAIN. 

In the syncline of Lookout Mountain, along the banks of 
Black Creek, are two well-known chalybeate springs. The first 
is near the end of the mountain, close to Alabama City on the 
Hollingsworth property, in the N. W. quarter, N. W. quarter, 
Section 32, Township 11, Range 6 E., and is known simply as 
the Chalybeate Spring. It flows in a small stream, strongly 
impregnated with iron, from beneath, the sandstone or con- 
glomerate which makes the falls of Black Creek. This water 



COAL MEASURES. 91 

has been Eavorabl) known for many years. No improvements 
have been made. Higher up the Valley, in Section 3, Town- 
ship to. Range 7 E., are the Lay Springs, where several bold 
streams of strong- chalybeate water flow from beneath a con- 
glomerate, probably overlying the one which makes' the falls 
below. 

At the lower end of Lookout Mountain, between Gadsden 
and Attalla, in the N. E. quarter, S. E. quarter, Section 31. 
Township 11, Range 6 E., is a sulphur spring of which it is 
difficult to tell whether it comes from the strata of the Coal 
Measures or from those of the Cambrian, since the two are 
there brought together by faulting. 

On the western side of Lookout Mountain numerous sulphur 
and chalybeate springs' issue from beneath the capping con- 
glomerate of the mountain. One such spring is east of Cordell 
station, on the Alabama Great Southern Railroad. 

M E X TONE SPRI XG S. 

The following analysis by Mr. Hodges is 'of water from a 
spring et Mentone, in Section 28, Township 5, Range 10 E., 
(Plate X, B), owned by the Loring Springs Hotel Company. 



Analysis of water from springs at Mentone. 



Parts per million. 

Potassium (K) 1.3 

Sodium (Na) 2.6 

Magnesium (Mg) ". 3.0 

Calcium (Ca) 4.5 

Iron (Fe) 8.6 

Alumina (AU0 3 ) 2.3 

Chlorine (CI) 8 

Sulphuric acid (SO*) 15.4 

Carbonic acid (HCO s ) 33.2 

Silica (Si0 2 ) 10.8 

80.5 



OTHER SPRINGS. 

On the west side of Wills Valley, in the N. W. quarter, 
Section 25, Township 6, Range 8 E.. under the cliffs of Rac- 
coon Mountain, a chalvbeate spring flows' from flagstones ly- 



92 DETAILS : APPALACHIAN DIVISION. 

ing between conglomerates. At the head of Bristow Cove, 
in Murphree Valley, two similar springs are recorded, one 
from above and one from below the lower conglomerate.- 

Across Raccoon Mountain and the Tennessee Valley, among 
the spurs of the Cumberlands in Jackson and Madison Coun- 
ties, many such springs come from die measures just below the 
conglomerates, as on Keel Mountain at Dr. Blair's residence 
in Section 30, Township 4, Range 3 E., and farther south in 
Township 5, Range 2 and 3, around the cliffs of the mountain. 
On Raccoon Mountain, also in Jackson County, near Fern Cliff 
Postoffice, a chalybeate spring arises from above the Cliff seam 
of coal. In Blount County, on the west side of the valley of 
Blount Springs, in the N. E. quarter, Section 10, Township 12, 
Range 2 W., and again on the east side of the same valley in 
the N. E. quarter, Section 19, Township 13, Range 2 W., are 
locally well-known chalybeate springs arising from the strata 
near the base of Coal Measures, like those above mentioned. 

In Winston County in a low place near Brown Creek in 
Section 3, Township 11, Range 9 W., is the Blue Spring of 
Dr. Kaiser, a sulphur spring of fine quality. In the so-called 
rock houses of Winston and Marion counties chalybeate springs 
are numerous and characteristic. 

In Tuscaloosa County in the N. E. quarter, Section 8, Town- 
ship 18, Range 9 W., in Wyndham Springs. This is a sulphur 
spring of pleasant taste and .reputed medicinal quality. Near- 
by, in the northeast corner of Section 34, Township 17, Range 
9 W., is Hagler's, a strong chalybeate spring flowing from 
flagstones. In the N. E. quarter of Section 16, Township 18, 
Range 10 W., is a spring which is rather saline and from which 
some salt was made during the civil war. 

Comment has already been made on the common occurrence 
of chalybeate and other springs' in the wet heads of the little 
ravines in all parts of the basin region of the Warrior coal 
field, where they are shed by underlying impervious seams of 
coal and are thus good guides to the prospector for coal. Very 
few of these springs have been improved. 

ARTESIAN PROSPECTS. 

The sandstones and conglomerates are the permeable beds, 
and as they are interstratified with shales and generally lie in 



COAL MEASURES. 93 

nearly horizontal position or with but moderate clip, they afford 
in these respects the requisite conditions for artesian systems. 
In the smaller fields, the Coosa and Cahaba, as has been stated, 
the strata dip toward the southeast over the en- 
tire width of the fields, with the exception of a narrow belt 
along" the eastern borders, where they stand nearly vertical 
in the eastern limb of the unsymmetrical synclines. In the 
southwestern part of the Cahaba field the stratigraphic rela- 
tions are more complicated, but even there these conditions pre- 
vail over much territory. In the Lookout Mountain and War- 
rior fields the strata form shallow synclines, which as a whole, 
have a pitch to the southwest. The success of arte- 
sian borings in these areas therefore, would seem to depend 
chiefly on the permeability of the sandstones and conglom- 
erates. So far as the porosity of these rocks is concerned the 
case is similar to that of older rocks generally which have lain 
long buried beneath other strata — the pore space is likely to 
be diminished by deposition of mineral matter from the un- 
derground waters. Like all massive rocks, these are traversed 
by joints and fissures which afford passageways for the un- 
derground waters, but such passageways are uncertain and 
unreliable. On these accounts it is generally not possible to 
forecast with any degree of certainty the result of artesian 
borings. Flowing wells of large volume are, however, hardly 
to be expected. 

ETOWAH COUNTY. 

In this connection may be mentioned several interesting in- 
stances of successful wells near the end of Lookout Mountain, 
where the prospects, on general principles, would appear to be 
unfavorable. At Alabama City a well 6 inches in diameter was 
bored about six years ago in the vertical rocks of the great fault 
which cuts off Lookout Mountain on the south. These rocks 
are the sandstones and shales of the lower Coal Measures. The 
well is 165 feet deep and is cased to the bottom. The well mouth 
is about 60 feet above the railroad track at the station, and the 
water stands at 30 feet. A pump delivering 12 gallons per 
minute has raised from this well 10,000 gallons without any 
diminution in the amount discharged, but whether the stand 
in the well was lowered could not be told. 



94 DETAILS : APPALACHIAN DIVISION. 

At the southeastern angle of the mountain rim overlooking 
Gadsden, at the residence of Messrs. T. S. Kyle and E. T. 
Schuler and the hotel, wells have been sunk into- the sand- 
stones or conglomerates which make the highest points of the 
mountain here and are 500 feet or more above the court-house. 
Mr. Kyle's well is within 200 feet of the edge of the escarp- 
ment, and though only 60 feet deep it furnishes an abundant 
supply of water, which is raised by a hot-air pump. Mr. Schil- 
ler's well is. in a similar position and 50 feet deep, furnishes an 
abundant supply, but perhaps not so much as the preceding. At 
the hotel also there was no difficulty in getting a good water 
supply in these sandstones. In all cases' the water rises in the 
wells, but does not overflow. The wells are sunk in the out- 
crop of the intaking rocks. 

On the N. C. and St. L. R. R. at Carlisle, on Sand Moun- 
tain, a fine stream of good water comes from a boring made 
in search of coal. Depth about 175 feet. No details obtained. 

C ah aba Field. 

ST. CLAIR COUNTY. 

At Davis Station, on the Seaboard Air Line, there is a flow- 
ing well, 31-2 inches in diameter and 244 feet deep, that yields 
about 25 gallons per minute. The well is in Section 7, Town- 
ship 16, Range 2 E., on the eastern side of the railroad, and is 
between the outcrops of the Wadsworth and Mammoth coal 
mines. 

Ware [or Field, 
walker county. 

At Oakman, Walker County, a well was bored in August, 
1899, during a long-continued dry spell. The depth was 58 1-2 
feet ; the boring was through sandstone, in which the water was 
obtained. The water rises two feet above the surface and the 
flow is about two gallons per minute; the temperature is' 63°F. 

At Jasper J. B. Carrington drilled two wells. No. 1 in Court 
House Square, Went to' the depth of 350 feet, but a good flow 
was obtained at 152 feet in a white sandstone. The water rose 
17 feet above the surface and continued to flow till the second 
well was drilled, when the stand went down to 15 feet. No. 2 



COAL MEASURES. 



95 



well, inches in diameter, was drilled at the coke ovens, getting 
a good flow ai [82 feet below the surface, which was here about 
25 feet lower than the surface in the court-house yard. The 
water rose 22 feet above the surface and is sufficient in quan- 
tity to supply water for 300 coke ovens. A pump with 6-inch 
suction pipe could be worked steadily on this well for fifteen 
hours, and then after a rest of five or six hours could be run 
another fifteen hours. 

At Stovall's gin. between the two wells above mentioned, a 
shallow well was dug in which, at the depth of 15 feet, water 
was' struck which rose to the surface and flowed off as a spring. 

CULLMAN COUNTY. 

At Cullman, the county seat, a number of wells were bored 
during the eighties, of which the following records have been 
furnished by Mr. Max Schmitt, of that town. There has been 
no diminution in the supply of any of these wells since the first 
tests. 

RECORD OF WELLS AT CULLMAN. 



No. 



Location. 



Depth W r ater evel 
Feet. Feet. 



Yield. 



1 1320 

2. City well .715 

3. Frank Ardt's place of business 96 

4. Cullman Cotton Oil Co.'s plant 100 

5. A. Dreher & Co.'s furniture factory 108 

6. C. Arnold & Son's factory 143 

6a. 30 feet from No. 6 100 

7. J. H. Carter's place of business 270 

8. George H. Parker's residence 101 

9. Paul Mohr's residence 110 

10. William Blevin's residence 78 

11. St. Bernard College 150 

12. St. Bernard College 209 



80 



63 

30 
80 
40 
40 
20 
46 
42 
48 
101 
130 



Abundant; level 
not lowered by 
steam pump. 

Level not lowered 
by large air com- 
pressor. 

Supply unlimited. 



Supply unlimited. 
Supply limited. 
Supply limited. 
Supply unlimited. 
Supply limited. 
Supply good. 
Supply plentiful. 
Inexhaustible. 
Supply unlimited. 



96 DETAILS : APPALACHIAN DIVISION. 



MAEION COUNTY. 



At the Brilliant coal mines of the Aldrich Coal Mining Com- 
pany two wells have been bored by J. O. Hefiin, as follows : 

Well No. I, bored in August, 1902; diameter, 8 inches; 
depth, 401 feet: yields', 250 gallons per minute for four hours; 
well has been in daily use day and night for three years ; tem- 
perature, 54°. 

The composition of the water from this well is shown in 
the following analysis by Mr. J. C. Long.* 

Analysis of water from well No. 1, Brilliant. 



Parts per million. 

Sodium (Na) 2.69 

Magnesium (Mg) 17.03 

Calcium (Ca) 52.11 

Chlorine (CI) 4.16 

Sulphuric acid (SOJ 14.00 

Carbonic acid (HCO s ) 111.34 

Iron and alumina (Fe 2 03,Al 2 O s ) 2.57 

Silica (Si0 2 ) 13.96 

Undetermined 36.29 

254.15 



Well No. 2, bored in December, 1904; diameter, 10 inches; 
depth, 375 feet; has yielded 1000 gallons per minute for four 
hours ; not yet in regular use. 

The water in both these wells stands just at the surface of 
the ground, with slight overflow. 

JEFFERSON COUNTY. 

Borings for water supply were made in the summer of 1900 
at Pratt City by Messrs. Canfield & Irwin, of St. Louis. 

Well No. 1, on the ridge between the old No. 1 slope and the creek, 
and on the edge of the fault; depth, 354 feet; cased' 50 feet; 323 feet of 
4-inch discharge, and 308 1-2 feet of 1 1-3-inch air pipe; stand during dry 
weather,— 76 1-4 feet, falling on pumping to —80 or —85 feet; yield, 200 gal- 
lons per minute; water soft and pleasant to the taste. The boring passed 
through alternating strata of sandstone and slate of varying degree of 
hardness, and a 4-foot seam of coal at 320 feet. 

Well No. 2, 1C0 yards west of No. 1; depth 405 feet; has not been satis- 
factory and is now seldom used. 

*Expressed by analyst in grains per gallon and hypothetical com- 
binations; recomputed in ionic form and parts per million at U. S. 
Geological Survey. 



COAL M L "iSURES. 97 

Two oilier wells nia\ be noted in this vicinity. In the N. E. 
quarter, X. E. quarter, Section 20, Township 17, Range 3, \V. 
the Pratt Company has a well 111 which a flow was obtained at 
65 feet, but lost at 500 feet. The well was plugged at 85 feet 
and lias since maintained a slight flow. In the S. E. quarter 
X. E. quarter of the same section Air. W. A. Brown, of Elyton, 
has a well 200 feet deep, which has a good flow. 

In section 26, Township 18, Range' 8 west one mile above 
the mouth of Indian creek, a boring was made to the depth of 
640 feet prospecting for coal. From this boring comes over- 
flowing water which fills an inch pipe. Along with the water 
is also inflammable gas. 

FAYETTE COUNTY. 

Only one artesion record is available from Fayette County. 
A well was bored in 1900 by \Y. F. Little at the court house, 
Fayette. Depth, between 500 and 600 feet. Between 200 and 
300 feet a seam of coal 4 feet thick was struck. No water was 
obtained. 

TISCAI.OOSA COUNTY. 

In the city of Tuscaloosa and a few miles above, at Holt, 
on the banks of the river, artesian wells have been bored into 
the sandstones and rocks of the Coal Measures with success, 
while at Kellerman. about 20 miles northeast, a boring to the 
depth of 1000 1-2 feet failed to get water. 

At the hosiery mills' in the suburbs of Tuscaloosa, is the well 
of Rosenau Brothers, drilled by Heflin Brothers in 1903. Its 
depth is' 520 feet; diameter, 6 inches; water obtained at 325 
feet rises to within 14 feet of the surface; ^sed in the mills; 
good drinking water; analysis is below. Record: Soil, o to 
20 feet; quicksand and gravel, 30 to 115 fe^t ; thence to bottom 
of the boring alternations of sandstones and slates of the Coal 
Measures, reported by the drillers to be limestones' and cherts. 
At another boring, however, for Mr. B. Friedman, at the site 
of his proposed furnace only a few miles distant, a drilling to 
the depth of 1000 feet showed no limestone or chert, but onlv 
sandstones, slates, and coal. 



98 details: Appalachian division. 

The analysis of the hosiery mill water, by Mr. Hodges, is 
as follows : 

Analysis of water from Hosiery-mill well, Tuscaloosa. 



Parts per million. 

Potassium (K) 5.9 

Sodium (Na) 403.7 

Lithium (Li) trace. 

Magnesium (Mg-) : 14.9 

Calcium (Ca) 70.0 

Iron (Fe) .5 

Chlorine (CI) 703.0 

Sulphuric acid (S0 4 ) 2.2 

Carbonic acid (HCO a ) 152.1 

Silica (Si0 2 ) 17.3 

1369.6 



The water from the hosiery-mill well* is much used by the 
people of Tuscaloosa and is reputed to have decided medicinal 
qualities. 

The well at Kellerman, on the property of the Central Coal 
and Iron Company, also bored by Heflin Brothers in 1903, to 
a depth of iooo 1-2 feet into the strata of the Coal Measures 
consisting of sandstones, shales, and four seams of coal, did 
not get water in any useful quantity. This may be, in part at 
least, due to the altitude, which is 500 to 600 feet above tide. 

The other well mentioned above, at the Friedman furnace 
site near Tuscaloosa, passed through similar strata to a depth 
of 1010 feet. No record is made of the water in this well, 
which was, however, bored for the purpose of prospecting for 
the underlying coal. It is quite probable that it would yield 
water, as the altitude of the mouth of the well is' not much 
above that of the hosiery mill. 

Tuscaloosa City well. In the summer of 1905 a boring was 
made by the city near the Court House to the depth of 151 1 
feet, Mr. Heflin being the contractor. Diameter of well, 8 
inches. Depth to solid rock about 90 feet. The casing went 
down into the rock ten or fifteen feet. No reliable record of the 
strata passed through is available, but the measures below the 
surface covering of sand and clay as s'hown elsewhere in the 
vicinity in other borings are the usual succession of sandstones 
shales, conglomerates, etc. of the Coal Measures, The water 
rises in the well to— 65 feet and is by estimate lowered by pump- 



COAL MEASURES. 99 

ing to— 150 feet, and the estimated yield is 15,000 gallons' a 
day. 

Three miles up the river from Tuscaloosa, at the furnace of 
the Central Coal and Iron Company, five wells were drilled in 
1903 by Heflin Brothers. No. 1 well was 544 feet deep ; No. 
5, 200 feet deep; and Nos. 2, 3, and 4 were of intermediate 
depths. No. 1 yields 50 gallons per minute ; No. 2, 85 gal- 
lons ; No. 3, 150 gallons; No. 5, about 200 gallons. Measure- 
ments were made by testing one well at a time. Water was 
found about 60 feet below the surface. No advantage was 
secured by lowering the water in the wells below 70 feet, 
and when this was done water could be heard running into the 
well. The water-bearing sand rock is about 89 feet above sea 
level. No decrease was observed in No. 2 after No. 5 was 
bored, and it is' not known what, if any, effect Nos. 3 and 4 have 
on No. 5. The water is used for drinking purposes alone, as 
it carries too much salt to be used in the boilers, which are 
supplied from the river. 

The water from well No. 1, which is on the hill near the 
Semet-Solvay ovens and which is much deeper than the others, 
is quite similar to that from No. 5, as may be seen by the analy- 
sis' below : 

Both analysis by Mr. H. Buel,* Chemist of the Central 
Iron Company. 

Analyses of water from wells at Holt. 



Parts per million. 

No. 1 No. 5 

Sodium (Na) 152. 63 177.93 

Potassium (K) 8.17 12.71 

Magnesium (Mg) 31.12 28.11 

Calcium (Ca) 84.00 80.97 

Chlorine (CI) 449.25 474.49 

Sulphuric acid (S0 4 ) 5.43 5.55 

Carbonic acid (HCO a ) 24.09 26.69 

Iron and alumina (Fe 2 03,Al 2 03) 13.69 13.01 

Silica (SiOo) 75.52 86.80 

Organic matter 103.90 106.47 

Hydrogen sulphide (H 2 S) 1.54 



947.80 1012.76 



*Expressed by analyst in grains per gallon and hypothetical com- 
binations. Recomputed to ionic form and parts per million at U. S 
Geological Survey. 



100 DETAILS: APPALACHIAN DIVISION. 

VALLEY OF THE TENNESSEE. 

SURFACE FEATURES. 

In the geologic sketch it has been shown that the Tennessee 
Valley in Alabama is of two fold character. The stretch from 
the northeast corner of the State down to Guntersville belongs 
to the Appalachian valleys already considered, and only that 
part of the State in which the river has a westerly course is' to 
be included in the present division. As stated, the strata are 
mainly lower Carboniferous limestones, with their intercalated 
sandstones near the top of the series. The lower sandstones of 
the Coal Measures cap the limestone east of Huntsville, but 
areas where this is the case would belong rather to the preced- 
ing division. 

SHALLOW WATERS. 

In the Tennessee Valley proper, therefore, the strata have a 
gentle dip toward the south, and, except at the western edge 
of the region, the rocks are covered by residual matter result- 
ing from their decay. This covering consists of clays and loams, 
with numerous' angular fragments of chert — the broken-up 
remnants of the chert layers with which the limestone are so 
generally interbedded. Good supplies of surface water from 
springs and open wells are to be looked for except where the 
soil is too thoroughly underdrained into the caverns and chan- 
nels of the omnipresent limestones ; but the water which finds 
its' way into these caverns emerges again as "big springs," of 
which those at Huntsville (Plate II.) and Tuscumbia (Plate 
XI) are the most famous examples. From the nature of the 
materials with which they come in contact in their underground 
passage, these waters are generally more or less highly charged 
with carbonate of lime and carbonate of magnesia. 

The area north of the river, extending from the Tennessee 
line southward for about 15 miles, underlain by the more sili- 
ceous limestones, has more abundant surface or hillside springs, 
while the red lands in the immediate valley of the river, as well 
as those South of Little Mountain in Moulton Valley, are rather 
characterized by lime sinks, caves, and big springs'. The depth 
of the surface soils, however, in both divisions insures a fairlv 
abundant supply of underground water. 



VALLEY OF THE TENNESSEE. 101 

M [NERAL WATERS. 

ClIAI VIJKA TV. Sl'U 1 N(1S. 

These arc perhaps the most numerous of the mineral waters 
of this as well as of other sections. They are common at the 
base of the capping sandstones of the spurs of the Cumber- 
lands east of the Huntsville meridian, and especially where a 
coal seam underlies. 

In the upper or Chester or Bangor limestone division of the 
Subcarboniferous one or two thick beds' of sandstone are in- 
tercalated between the limestones, and at the contacts of the 
two rocks mineral springs are often seen, the most numerous 
of these being the chalybeate, though sulphur springs also 
occur. Examples of these are the Ligon Springs, in the north- 
west corner of Township 6, Range 1 1 W. ; and the Franklin 
Springs, in Section 16, of the same township and range. 
According to Professor Tourney's analysis of the water of the 
Ligon Springs, it contains free carbonic acid, sodium chloride, 
sulphate of iron, and a trace of sulphate of magnesium. 

In the immediate vicinity of this spring is another containing 
chloride and sulphate of iron and free carbonic acid. At the 
Franklin Springs, besides the sulphur springs for which the 
place is noted, there is a chalybeate spring which, according 
to Professor Tourney, contains in addition to the iron only a 
little lime. 

At the base of the Bangor limestone, where it is contact with 
the St. Louis limestone, is another horizon of the chalybeate 
waters, which break out in many places at the foot of Little 
Mountain. 

Lastly, in die lowermost of the Subcarboniferous limestones 
which immediately overlie the Devonian black shale, chalybeate 
waters spring up in connection with sulphur waters but some- 
times alone. Of this class is the Pettusville Spring, in the S. E. 
quarter Section 10, Township I, Range 4 W. 

Sulphur Springs. 

While the chalybeate springs are more numerous the sul- 
phur springs are generally more valued as places of res'ort for 
health and pleasure seekers. The most important of these 



102 details: Appalachian division. 

springs in the Tennessee Valley, as elsewhere in the Appa- 
lachian division, have their origin in the Devonian black shale, 
because of the organic matter and pyrite nodules which it con- 
tains ; and it is easy to understand why chalybeate springs are 
often found associated with sulphur waters, from this source. 
The exposures' of the black shale in this area are mostly con- 
fined to Elk River, Limestone Creek, and the headwaters of 
Flint River, all in the extreme northern part of the State. 

The Moore Spring, 12 miles north of Athens, on Maple 
Creek, a tributary of Elk River, according to Professor Tourney 
had a temperature of 68 degrees, while the atmospheric tem- 
perature was 71.6 degrees. The water contains, besides the 
sulphur, free carbonic acid, carbonate of lime, sodium chloride, 
and traces of carbonates of iron and potassium. 

The Wooley Springs, in the S. W. quarter Section 39, Town- 
ship 1, Range 3 W., once much visited but now practically 
abandoned, include a chalybeate and an alum spring in addi- 
tion to the white sulphur spring. 

The Johnson well, near Meridianville, in Section 26, Town- 
ship 2, Range 1 W., is one of the best known springs in this 
section. It also embraces, in addition to the sulphur springs, 
an alum spring. This spring is on a tributary of Flint River 
and appears to rise from the lower Subcarboniferous' limestones 
and not from the black shale. 

Another sulphur spring, on Barren Fork of Flint River, in 
the S. W. quarter Section 26, Township 1, Range 1 E., is as- 
sociated with a chalybeate spring. 

At New Market, in the S. W. quarter, N. W. quarter Sec- 
tion 33, Township 1, Range 2 E., a well was bored for oil to a 
depth of 1000 feet or more. In this well sulphur water was 1 
struck at a depth of 1 18 feet and again at 700 feet. The water 
rises above the surface and is used by the inhabitants of the 
town. 

Stewart's well, near Florence, was examined by Professor 
Tuomey, and found to contain, in addition to the sulphur, free 
carbonic acid, s'odium chloride, and sodium carbonate, with 
traces of magnesium carbonate and alumina. 

Another horizon of sulphur waters is that mentioned above 
for chalybeate waters, viz, the contact of the intercalated sand- 
stone beds and the limestone in the upper Subcarboniferous 
or Bangor group. At Franklin Springs, in Section 16, Town- 



VALLEY 01? THE! TENNESSEE. 103 

ship (>, Range 11 W., already mentioned under "Chalybeate 
springs." is a sulphur spring. Again, at the base of Little 
Mountain sulphur and chalybeate waters are seen near Town 
Creek station, on the Southern Railroad. 

Farther east, in Morgan County, in the southeast corner of 
Section 19, Township 6, Range 1 W., are the Valhermoso 
Springs, two sulphur and one chalybeate, similarly situated 
geologically at or near the contact of the sandstones with the 
limestones. 

Alkaline-saline Springs. 

In Lauderdale County, near the banks of Shoal Creek, are 
many springs which have attained some reputation. The best 
known of these is Baile3' Springs, (Plate XII) consisting of a 
group of springs with water of varying quality. A sample of 
the water from a spring recently improved by Dr. H. A. Moody, 
below those 'shown in plate, has been analyzed by Mr. R. S. 
Hodges, with the result below : 

Analysis of water from Moody's Spring at Bailey Springs. 



Parts per million. 

Potassium (K) 1.4 

Sodium (Na) 2.4 

Magnesium (Mg\) 2.6 

Calcium (Ca) 16.0 

Iron and alumina (Feo03,Al 2 : >) 1.6 

Chlorine (CD 5.3 

Sulphuric acid (SO*) 3.8 

Carbonic acid (HCO a ) 57.0 

Silica |Si0 2 ) 8.1 

98.2 



Other springs here are called chalybeate and iron springs and 
are reputed to have special curative qualities. The grounds' at 
Bailey's are well kept and the accommodation is ample for a 
large number of guests. Much of the patronage from a dis- 
tance comes from Memphis and other points to the west in Miss- 
issippi. 

The small house or pavilion in the foreground of Plate XII 
is over the "Rock Spring." 

Professor Tuomey mentions several other springs in the same 
general region, viz., Todd's, Lee's, Langford's, Witherspoon's, 



104 details: Appalachian division. 

etc., but none of these, so far as the writer is aware, is now 
fitted up for the accommodation of visitors. 

Acid Springs. 

At center Grove, in Morgan county, W. E. Forman has a well 
with strongly saline water of acid reaction and peculiar com- 
position, as may be seen from the subjoined analysis by Mr. 
Hodges : 

Analysis of water from W. E. Forman's well, Center Grove. 



Parts per million. 

Potassium (K) trace. 

Sodium (Na) trace. 

Magnesium (Mg) 2S.2 

Calcium (Ca) 23.8 

Manganese (Mn) 26.6 

Iron (Fe) 7.1 

Aluminum (Al) 7.9 

Chlorine (CI) trace . 

Sulphuric acid (S0 4 ) 276.0 

Carbonic acid (HC0 3 ) trace. 

Silica (Si0 2 ) 50.0 

419.6 



The large portion of manganese sulphate is exceptional 
among the waters thus far examined, and the presence of 
the sulphates, especially of magnesium, make it also a strongly 
alterative water. 

Tab Springs. 

An account of the mineral springs of the Tennessee Valley 
would be incomplete without some mention of the tar springs 
which occur in connection with the upper Subcarboniferous or 
Bangor limestones of Moulton Valley. The westernmost of 
these is reported in Section 27, Township 5, Range 15 W., near 
the State line of Mississippi ; but the best known are the Capps 
Creek tar springs, in the lower part of Lawrence County, in 
the S. W. quarter Section 6, Township 8, Range 6 W., once 
much visited by the afflicted, who drank tar water or took 
pills of the somewhat indurated tarry matter. 

On Town Creek, in the N. E. quarter Section 16, Township 
5, Range 9 W., and again in the N. E. quarter Section 33, 



VALLEY OF THE TENNESSEE. 105 

same township and range, an din the X. \Y. quarter Section 
Township 6, Range 9 \\\, arc tar springs, at all or most of 
which borings have been sunk for oil. 

Tn all this region the wells mentioned often yield rulphur, 

chn!\ ! c;te, and salii-e waters, and sonic of them overflow, as 
will b emore particularly noted in the next section. 

ARTESIAN PROSPECTS. 

From the general account of the geologic structure above 
given, the outlook for artesian waters might be expected to be 
fairly good, and the few wells that have been bored or of which 
records have been obtained, bear out this expectation. As has 
been intimated, the limestones' are generally inferior water 
bearers. Their capacity in this respect depends largely on 
the existence of fissures and joints and on other secondary 
characters which cannot be recognized at the surface. The 
almost universal presence of chert in these limestones is' a fa- 
vorable circumstance down to certain depths, for the leaching 
out of the calcareous parts by circulating waters leaves the 
chert as an exceedingly open and porous residue. 

Beds of open-textured sandstone also lie intercalated be- 
tween the limestones prevailing in the territory south of the 
river, or rather south of the range known as Little Mountain, 
in Moulton Valley. Many borings have been made in this ter- 
ritory in search of petroleum and many also probably for water, 
with reasonable success, though flowing wells are comparatively 
rare. 

New Market. 

Very few records are available of borings north of the river 
— only those of the New Market well in the S. W. quarter N. 
W. quarter Section 33, Township 1, Range 2 E. and of two 
wells at Hazel Green, near Huntsville. all of which were bored 
for oil. 



106 DETAILS : APPALACHIAN DIVISION. 

The record of the New Market well is as' follows : 
Record of New Market Well. 



Feet. 

Soil 8 

Cherty rocks 25 

Limestone and chert 30 

Black shale 18 

Gray sandstone 2 

Limestone and shales 965 



In this well the Subcarboniferous group is represented by 
the first three of the series, the Devonian by black shale and 
sandstone and the Silurian by limestones with shale parting. 
The well was bored in 1890, with diamond drill; diameter, 2 
inches ; permanent fresh water was struck at 22 feet and sulphur 
water at 1 18 and 700 feet. No salt water or gas was' found. The 
sulphur water from both depths mentioned flows above the sur- 
face and is used by the inhabitants of the town. 

Hazel Green. 

Of the wells on Overton farm, near Hazel Green the fol- 
lowing records were obtained. 

"Well No. 3, first water struck at 60 feet: yield, 40 gallons per minute; 
stand,— 20 feet; temperature, 52 degrees. At 187 feet a black sulphur 
water was struck, and at 217 feet a strong salt water. No water was ob- 
tained below 271 feet, to which depth the casing extends. The mouth of 
the well is 667 feet above tide. 

Well No. 4, depth, 310 feet; first water at 32 feet, in rock; water does 
not flow, but stands at ground level except when gas is turned in, when 
it is blown about three feet above the surface; yield, 150 gallons per 
minute, without any perceptible lowering of the stand; temperature, 56 
degrees. In this well neither sulphur nor salt water was struck and no 
water was found below 147 1-2 feet. The mouth of the well is 603 feet 
above tide. 

These wells were bored for oil and gas. The quantity of the 
latter from well No. 4 is sufficient to run a 25 horse power 
boiler. 

SOUTH OF TENNESSEE RIVER. 

South of the river the borings are very numerous. 
Curtis well, about 6 miles southeast of Decatur ; bored about 
seventy-five years ago ; depth, 341 feet ; flow, about 10 gallons 



VALLEY OF THE TENNESSEE. 3 07 

per minute, which has been constant in quantity since the well 
was drilled; water slightly impregnated with sulphuretted h\- 
drogen gas. 

Judge H. B. Tompkin's well. — About 2 miles east of Sheffield 
recently bored; depth, 190 feet; 50 feet through soft surface 
earth. 25 feet through chert, and the rest through dark flint; 
water rises about 48 feet in the well and is raised to the surface 
by windmill pump; — supply plentiful. 

L. W. Deprez's well, at Russellville ; depth, 60 feet; the water 
rose about 38 feet in the well. 

E. M. Harris's well, 4 miles southeast of Russellville ; depth, 
about 100 feet; water rose to within 15 feet of the surface. 

The numerous borings, some of them to the depth of more 
than 1700 feet, which have been made in search of oil and 
natural gas have in most cases yielded salt water. As has been 
mentioned above these wells are most common in the country 
about Aloulton and Russellville, since it is here that the tar 
springs abound, and these have been selected as the most prom- 
ising places for borings. The Goyer wells, in Section 29, 
Township 7, Range 6 W. are perhaps the best known. The well 
at Hartsell, 1730 feet deep, found fresh water at 30 feet, sul- 
phur at 160 feet, brackish water at 352 feet, and salt water at 
1730 feet. A salt well in the southeast corner of Section 10, 
Township 7. Range 5 W. has a depth not accurately ascertained 
but propably less than 200 feet. The water overflows, as it 
does also in some of the wells in Moulton Valley. However, 
the writer knows of no well in this region which has been sunk 
for water, oil being the thing sought. While little account has 
been taken of the water obtained in these borings it is probable 
that all of them have a supply sufficient for ordinary purposes, 
if the quality be suitable, but in only a few of them does the 
water rise above the surface. 



COASTAL PLAIN DIVISION. 

General Account. 

The general topographic and geologic features of the Coastal 
Plain, which embraces about three-fifths of the area of the 
State, have been sketched above in Chapter II ; but since most 
of the artesian wells of the State (more than 95 per cent, of 
those recorded in this report) are in this territory, it is desir- 
able that the stratigraphic relations of the formations be pre- 
sented somewhat more in detail. 

For shallow waters this division, like the Appalachian, is de- 
pendent in part on the residual materials provided by the decay 
of the underlying stratified rocks ; but in addition to these a 
thin coating, 25 or 30 feet in thickness, of loam, sand, and peb- 
bles — the Lafayette formation post-Tertiary age— has been 
spread unconformable upon the Cretaceous and Tertiary strata 
over the entire Coastal Plain ; and where these deposits have 
not been carried away by erosion they, of course, determine the 
s'urface-water conditions in much greater degree than do the 
residual soils of the Cretaceous and Tertiary. 

In the southern part of the State, as indicated by the map, 
(PI. 1.) another formation, in many respects similar to the La- 
fayette but older, covers great areas of the St. Stephens and 
post-Eocene formations down to the borders of the sea. This 
is the Grand Gulf formation, which will be treated in detail la- 
ter. 

The artesian systems of the Coastal Plain are provided by 
the strata of the Cretaceous and Tertiary formations. The 
general stratigraphic relations of these formations are shown 
in fig. 21, p. 62. 

In the great area embraced by the Coastal Plain, uniformity 
in the artesian conditions of the same formation in different 
parts is not to be looked for nor does it exist. In' consequence, 
it will be expedient' to give the notes on wells', etc., under sev- 
eral heads, those in which the conditions are approximately sim- 
ilar being grouped together. It will also be expedient to dis- 
cuss the subject by counties, following in general a geographi- 
cal order. It should be understood, however, that in the very 
nature of things this dual arrangement can not be followed ab- 



GENERAL ACCOUNT. 109 

solutely, for the conditions arc not identical in any two conn- 
ties. 

The wells' which derive their water supply from the Cre- 
taceous strata fall naturally into two groups, which, in geo- 
graphical distribution, coincide approximately with the drain- 
age areas of Tombigbee and Alabama rivers on the west and 
that of the Chattahoochee on the east. The Cretaceous well 
records by counties will he given in these two groups, preceded 
by such additional details of the stratification as may he neces- 
sary for the fuller understanding of the artesian conditions. 

The Tertiary wells are few in number as compared with the 
Cretaceous. They will constitute a third group and their de- 
scription by counties will also be proceeded by such addition- 
al explanatory details of stratification as can be obtained. 

The geographical distribution of the wells of the Coastal 
Plain is shown, at least approximately, on the geologic map 
(PI. I.) The marks indicate the locations' of groups of wells 
rather than of individual wells, it being manifestly impossible 
on a small scale map to mark each of the 1414 wells of which 
reci irds have been obtained. 

From this map it will be apparent that most of the wells 
are on the outcrop of the Selma chalk (prairie region). These 
get their water supply mainly from the Entaw sands, but some 
of the deeper borings, especially those near the northern bor- 
der of the chalk, penetrate into- the still lower Tuscaloosa strata, 
also water bearing. 

The wells on the Eutaw outcrop get their water in part from 
the Entaw and in part from the Tuscaloosa, according to depth, 
while those located on the Tuscaloosa formation begin and end 
in it. 

South of the chalk are some wells, both in the Cretaceous 
and in the Tertiary, which derive their water supply from the 
uppermost Cretaceous (Ripley, or Bine Marl) strata. This is 
especially the case in the eastern counties — Pike, Bullock. Bar- 
hour, and Russell. 

The following figures will show perhaps more clearlv than 
does the map the concentration of the wells in Cretaceous 
strata. Of the whole number (1414) of which accounts are 
given herein. 1.220, or a little over 86 per cent, are in the Cre- 
taceous, while only 136, or not quite 10 per cent., are in the 



110 ' details: coastal plain division. 

Tertiary, the remaining 4 per cent, being in the older forma- 
tions of the Appalachian division. 

The map and figures will further show the crowding of the 
wells in the Cretaceous counties west of Lowndes, viz, Dallas, 
202; Perry, 79; Marengo, 49; Hale, 192; Greene, 323; Sumter, 
59; and Pickens, 94; making 998, or something more than 70 
per cent, of the whole number recorded. In these counties 
there are also many old wells bored before the war and now 
abandoned or fallen into decay, of which it is impossible to get 
any information, and the records' are therefore defective, ex- 
cept in the case of Greene County, where Judge G. B. Mobley, 
of Eutaw, for many years past greatly interested in the sub- 
ject, has collected notes from which it has been possible to get 
a nearly correct list of that county. 

In the Tertiary area there is no similar concentration any- 
where, nor is the whole number of wells very great — 136. It 
will be seen that most of the borings follow the railroads, the 
exceptions being mainly the wells recently sunk in search of 
oil, e. g., in the s'alt-wells region of Washington and Clarke 
and the lower parts of Mobile and Baldwin counties, and at 
Citronelle, Mobile County, and Roberts, Escambia County. 

In the salt-wells region referred to, as in parts of the Cre- 
taceous' prairie region, there are many old wells sunk years ago 
of which no records are now obtainable, indeed, the very loca- 
tion of many of them can not be ascertained. 

Most of the artesian wells in the Tertiary section obtain their 
supply from the great sandy Nanafalia formation and its ad- 
jacent Tuscahoma above, and Naheola below. A few, like those 
at Geneva, get water in the Claiborne or Buhrstone. At Brewton 
the shallow wells, less than 100 feet in depth, probably do not 
go deeper than the Grand Gulf, which there forms the surface ; 
but the deep borings get water in the St. Stephens strata. 

The deep wells in Mobile and Baldwin counties, starting in 
Grand Gulf strata at the surface, bring up from depths of 700 
to 1550 feet, shells characteristic of the Miocene formations 
exposed along the banks of the Chattahoochee river and first 
brought into notice by D. W. Langdon, of the Alabama Geo- 
logical Survey. The outcrop of these Miocene formations 
in Alabama has as yet been observed at only one point, i. e., 
near Roberts', Escambia County, on the banks of Conecuh river. 



GENERAL ACCOUNT. 11 1 

but exposures are numerous just across the line in Florida, at 
Oak Grove and other localities. 

The flowing wells of the Coastal Plain are practically con- 
fined to the lowlands, the low relief precluding- the possibility 
of any great hydrostatic head. As a consequence, wells of this 
kind are not numerous outside of the great river valleys. 

The accopanying sketch map (PI. XIII.) shows approxi- 
mately the artesian systems as they have been outlined above. 
It will be seen that the wells in the Tertiary are not numerous 
enough or sufficiently well distributed to make it possible to 
outline the separate basins', as can be done in the Cretaceous. 
Marks, however, are attached to all the artesian well 
areas showing the formation from which it is probable the 
water supply comes. These indicate that the Nanafalia and 
the immediately adjacent sandy formations above and below it 
are the main source in the Tertiary, as the Eutaw stands are 
in the Cretaceous. 



Waters of the Cretaceous, 
to.mbigbee-alabama-conecuh rivers drainage. 



From about the meridian of Montgomery westward the Cre- 
taceous' strata in Alabama exhibit four well-marked divisions, 
which, in descending order, are as follows : 

i. A series of dark-gray or bluish sandy, micaceous clays 
which w r eather into yellow micaceous sands, impure limestones 
with many casts of fossils', then sandy strata again — in all be- 
tween 200 and 300 feet thick. This division has been called the 
Ripley, from a locality in Mississippi. 

2. An impure chalky, argillaceous limestone, or tolerably 
uniform composition, known as the Selma chalk. The thick- 
ness of this division is about 1,000 feet in the western part of 
the State and through Mississippi, but toward the east it thins 
down and is hardly to be distinguished east of Montgomery. 

3. A series of laminated sands and sandy clays', at least 300 
feet thick, known as the Eutaw formation. 

4. A great series, at least 100 feet thick, of variouslv colored 
sands and laminated massive clays, some of which are filled 
with the impressions' of leaves, often in a good state of preser- 



112 details: coastal plain division. 

vation. To this series, which is, in part at least, equivalent to 
the Potomac formation of the Atlantic coast, the name Tusca- 
loosa formation has been given. 

The Selma chalk, or "rotten limestone,'" as it was once call- 
ed, is deficient in surface waters except during wet seas'ons, 
and it is because of this and the fact that the best farming 
lands of the State — the black prairie lands — are derived from 
it that so large a proportion of the artesian wells are to be 
found located on this chalk. Especially is this true of 
the earlier wells, which were almost without exception in the 
prairie region. Recently, however, deep wells' have been sunk 
in other Cretaceous strata which are not lacking in surface 
water. 

In the western part of this drainage area the water-bearing 
formations are the Tuscaloosa and the 'Eutaw, which are pre- 
vailingly sands and clays in many alternations. The Ripley 
calcareous sands are also utilized to some slight extent in the 
western part, but they become more and more important in 
this' respect to the east, as will be seen below. 

In the Tuscaloosa formation the borings have been compar- 
atively few, and a general statement of the water horizons can 
not be made with certainty. At the summit of the formation 
there is usually a body of purple or red clay of considerable 
thickness through which the boring must go before water is 
reached. Mr. John I Hawk, of Selma, who has had much 
experience in this business, says' that when he strikes the "pink 
kaolin" he usually stops, as he is not likely to get water for at 
least ioo feet. In the lower part of the formation the borings 
have been more numerous, especially in Tuscaloosa County, 
where the records show that after a depth of 20 to 30 feet of 
loose materials', the borings go through 100 to 200 feet of what 
is called "blue rock," below which as a rule a supply of water is 
obtained. 

As regards the Eutaw sands the case is different, for by far 
the greater proportion of the artesian wells in Alabama derive 
their water from this horizon. Mr. John I. Hawk has fur- 
nished the following notes. Most of the wells bored by him 
have been in the Selma chalk area, this' being the "blue rock" 
of the well borers, but not the blue rock above mentioned in 
the Tuscaloosa formation. Mr. Hawk says: 



WATERS OF THE CRETACEOUS. 113 

"Once through the blue rock, we strike a sand rock varying from 1 to 
3 feet in thickness, and next, small beds of black and white sand with 
a green coloring in it (green sand) and interspersed with green soap- 
stone (laminated clay.) The first water is in these strata of sand, and 
it comes up according to the elevation; in very low placed it will over- 
flow, but it never makes a strong stream. 

"Prom 75 to 100 feet below the sand rock mentioned, we encounter a 
very hard rock (I think a white, lime rock), varying in thickness in dif- 
ferent sections from 2 inches to 2 feet; once through this rock we get 
the second stream of water in much the same kind of strata, and this 
water will rise about 12 feet higher than the first stream. 

"About 75 to 100 feet below the hard cover rock just mentioned, we 
have what we call white soapstone, from 10 to 40 feet in thickness; then 
a stratum of sand whiter and coarser than any of the preceding, inter- 
spersed with green soapstone and the same green coloring in the sand. 
This lied is from 40 to 75 feet thick and from it comes our third water, 
which rises about 10 feet higher than the second. 

"Immediately below this is a bed of green soapstone, from 50 to 50 
feet thick, followed by a marl from 20 to 50 feet thick, and beneath the 
marl we have a very coarse sand interspersed with sandrock and soap- 
stone, from 20 to 40 feet in thickness. In this we get our fourth stream, 
which rises from 30 to 40 feet higher than first stream and is very strong. 

"Below this the pink kaolin begins, there being about 400 feet or a 
little more between the blue rock and the pink formation. I have bored 
into this pink formation from 40 to 100 feet, but have never gone through 
it, nor increased the supply of water any by boring beyond the coarse 
white sand." 

In the eastern part of the area under consideration the drain- 
age is divided between Alabama and Conecuh rivers in Pike 
and Bullock counties, and the artesian characters in these two 
counties are transitional, having many points of resemblance 
to those of the Chattahoochee area in Russell and Barbour 
counties. 

DISCUSSION EY COUNTIES. 
LAMAR COUNTY. 

The surface formation in this county is the Tuscaloosa, with 
a capping of Lafayette sands and pebbles where erosion has 
not been too great. Underlying these two formations and ex- 
posed along the valleys of some of the streams in the northeas- 
tern part of the county are the sandstones and shales of the 
Coal Measures'. 

Shallow Waters. 

The sands and pebble beds and laminated clays of the Tus- 
caloosa and Lafayette formations afford here, as elsewhere, 

8 



114 details: coastal plain division. 

ample supplies of good surface water in springs and open wells, 
•and as a consequence few deep wells have been needed. 

Artesian Peospects. 

The s'awds and clays of the Tuscaloosa, in many alternations 
and with moderate and uniform westerly or southwesterly dip, 
furnish the requisite conditions for artesian systems, as is 
provided by the few wells that have been bored in the county 
and by those in the adjoining county in Mississippi, Monroe. 

SULLIGENT. 

Thus far records' have been obtained only of wells at Sulli- 
gent, where three were bored in 1900 by W. F. Little, of West 
Point, Miss. No record could be secured of the strata passed 
through in these borings. 

Town well, depth, 206 feet ; 3-inch iron casing at the bottom ; 
when first drilled flowed 74 gallons per minute ; In less than two 
years the casing was corroded and the well clogged so that the 
present yield (1904) is only 18 gallons; water rises to> 28 feet 
and still flows. 

Ogden well, 250 yards south of the town well and about the 
same depth ; is filled in and does not flow at present. 

Stone well, 250 yards east of the town well and about the 
same depth; still flows (1904). 

FAYETTE COUNTY. 

The stratigraphic conditions in Fayette County are prac- 
tically the same as those above given for Lamar County, ex- 
cept that the surface formations' (Tuscaloosa and Lafayette) 
the not present in quite so great thickness and the Coal Meas- 
ures appear in the valleys of most of the larger streams. What 
has been said concerning the surface waters and artesian pros- 
pects of Lamar will apply equally to Fayette County. 

The only artesian well in the County of which a record is 1 
available is at the court-house, Fayette, and was bored by W. 
F. Little in 1900. Its depth is between 500 and 600 feet. 
At 200-250 feet a seam of coal 4 feet thick was struck. The 
well was through rock and was abandoned without getting anv 
notable supply of water. 



waters oE the; cretaceous. 115 

This particular well, while starting in the Tuscaloosa forma- 
tion, soon reaches the Coal Measures', and has been mentioned 
under that head (p. 97). But further west in this county, the 
Tuscaloosa formation affords conditions similar to those re- 
ported above under Lamar County, and artesian boring's should 
succeed if proper localities are selected. The wells would, 
however, be shallow, since the rocks of the Coal Measures are 
nowhere very far below the surface in Fayette County. 

TUSCALOOSA COUNTY. 

Surface Features. 

Except in a narrow strip in the southeast corner of this 
county, where Subcarboniferous, Silurian, and Cambrian beds 
are exposed in the anticline of Roups Valley, the Coal Meas- 
ures should on general principles, underlie the entire county, 
but as a matter of fact these strata are not revealed either in 
outcrop or by borings southwest of a northwest-southeast diag- 
onal passing through the city of Tuscaloosa. Northeast of 
this line the sands and clays of the Tuscaloosa formation and 
the red loam and pebbles of the Lafayette form the surface, 
with the older strata outcropping in the low grounds of the 
streams. Only the two younger formations' are known in the 
southwestern half of the county, except along Black Warrior 
River, where the Second Bottom and other recent deposits 
occur. An account has' already been given (p. 97-99) of the 
surface and artesian waters of the Paleozoic half of the county, 
and this section is concerned only with the Cretaceous half. 

Shallow Waters. 

In the sands of the Cretaceous and especially in the loam 
and pebble beds of the overlying Lafayette a practically never 
failing supply of good water is recovered in open wells and 
springs. The former are rarely as deep as 100 feet, and the 
finest springs of pure water flow from beneath the Lafayette 
mantle. It would be impracticable to mention localities of the 
springs, since they occur almost everywhere that the contact 
of the Lafayette with an older formation is exposed in a ravine 
or bluff. The water, as a rule, is remarkably pure, with a small 
content of solid matter, and the same mav be said of the 



116 details: coastal plain division. 

waters of the open wells when they are sunk in Lafayette mate- 
rials only. Inasmuch as the Lafayette lies upon the eroded, 
uneven surface of the Tuscaloosa, the latter formation is often 
penetrated in wells, and when lignitic clays are struck in such 
cases the water frequently has' a brackish taste. 

The springs which flow from beneath the Lafayette gravel 
on the grounds of the University of Alabama may be taken as 
fairly representative of the class. Analysis of the water from 
one of these springs, made by Mr. Hodges, shows the following 
composition : 

Analysis of water from spring at University of Alabama. 



Parts per million. 

Potassium (K) .9 

Sodium (Na) , 1.8 

Magnesium (Mg) 1.6 

Calcium (Ca) ., 4.9 

Iron and Alumina (Fe 2 03,Al 2 3 ) .7 

Chlorine (CI) 1.9 

Sulphuric acid (SO4) 5.3 

Carbonic acid (HCO s ) 20.2 

Silica (Si0 2 ) 6.6 

43.9 



In some cases, while the total amount of mineral matter in 
these waters may be quite small, yet the relatively large pro- 
portion of some of the constituents may give to the water a de- 
cidedly mineral or medicinal quality. This may illustrated by 
the following analysis by Mr. Hodges : 

Analysis of water from Ozment Spring. 



Parts per million. 

Magnesium (Mg) 1 A 

Calcium (Ca) 2.3 

Iron and Alumina (Fe 2 03,Al 2 3 ) 2.0 

Chlorine (CI) trace 

Sulphuric acid (S0 4 ) 5.4 

Carbonic acid (HCO s ) 6.9 

Silica (SiQ 2 ) 17.9 

35.9 



Here the proportions of: Magnesium sulphate and of iron 
to the whole amount of solid matter are relatively very large, 



WATERS OF THE CRETACEOUS. 11 7 

and apparently justify the claim that this is a mineral water. 

Prof. J. H. Foster, of Tuscaloosa, has furnished the follow- 
ing notes concerning two "blowing wells" in the lower part 
of the county : 

The first of these wells' is on the old E. R. King" place, now 
owned by Air. J. C. Mize, in Fosters settlement, about 12 miles 
south of west of the city. The well is a bored well, 8 inches in 
diameter and 90 feet deep, with a circular plank curbing ex- 
tending about 3 feet above the ground. A hinged lid of board, 
about 10 inches wide and 12 inches long, fits over the top of 
the curbing. On the approach of a storm or of change from 
fair weather to foul, a strong current of air comes' from the 
well sufficient to lift the free end of the lid 3 inches, this lifting 
of the lid occurring at longer or shorter intervals according to 
the magnitude of the barometric change. Sometimes the lid 
will be raised and dropped with great rapidity making a rat- 
tling noise that can be heard at a distance. From the depths 
of the well come sounds as of a cauldron of water furiously 
boiling. Under ordinary conditions the water stands about 3 
feet deep in the well, but on the approach of storms', when the 
water is disturbed as above described, the bucket frequently 
comes up only half full. These disturbances in the well usually 
occur from twenty-four to forty-eight hours before a predicted 
storm. On the premises of Mr. J. N. Robertson in Hickman, 
about 3 miles west of Fosters is' another well which exhibits 
similar phenomena. 

Artesian Prospects. 

Northeast of the city of Tuscaloosa the Cretaceous beds 
occur in detached masses occupying summits only, and hence 
are not serviceable for artesian systems'. In the southwestern 
part of the county, however, they are continuous, and because 
of their composition (alternating clays and sands) and of their 
moderate and uniform dip, the conditions are in every way fav- 
orable to artesian wells. The fact that good surface water can 
so easily be had from the Lafayette beds in every part of the 
county has made recourse to artesian wells unnecessary, except 
in the Second Bottom lands of the river. Here are the earli- 
est artesian wells, and indeed the only ones, except those near 
Tuscaloosa which have been sunk into the strata of the Coal 



118 details: coastal plain division. 

Measures, as already described (p. 97-99). To those who- are 
compelled to live in the lowlands along the river, artesian water 
should prove a boon in diminishing the sickness which seems 
to follow the use of surface water in the river bottoms. The 
use of artesian water at the three locks next below Tuscaloosa 
is said to have effected a very great improvement in the health 
of the workmen. 

All the artesian wells in the Coastal Plain part of this county 
begin and end in the Tuscaloosa formation. 

Until about the year 1900 the only artesian well in the county 
was that at Willifords' Landing, on the river, mentioned below, 
but it has since been found that good artesian wells may be 
had in all the lowlands between Saunder's and Foster's ferries 
and thence on both sides of the river to the lower border of the 
county. Probably the impetus to this artesion boring was 
given by the action of the United States engineers in sinking 
wells' at the lock sites below the county line. Gradually bor- 
ings have been made farther and farther north, as success was 
achieved. 

TUSCALOOSA AND VICINITY. 

The following records show the present status of the sub- 
ject : 

S. F. Alston's well, in the N. E. quarter N. E. quarter Sec- 
tion 15, Cownship 22, Range 11 W. ; bored in 1902 by Martin 
& Morriscn; depth, 268 feet (Alston), 234 feet (Morrison); 
original volume, 75 to 100 gallons ; ran thus' six months until 
Mr. Foster's well (see next record), a half mile away, was 
bored, when it fell off gradually to its present volume, 3 gal- 
lons ; temperature 66 degrees ; water rose 16 feet above the 
surface and overflowed with small force; 

Record of S. F. Alston's well, Tuscaloosa. 



Feet. 

Clay, etc — 6 

Dark sand 6 — 05 

Blue rock 50 — 236 

Sand, water bearing- 236 — 268 

First overflow from 236 feet; 3 — inch casing- down to blue rock. 



WATERS OP THE CRETACEOUS. 119 

J. Manly Foster's wells: No. 1. in the S. E. quarter N. E. quarter Sec- 
tion 15. Township 22, Range 11 W., half a mile from the Alston well; 
bored in 1902 by W. V. Morrison; depth, 234 feet; 3-inch casing; flowed 
strong stream for six weeks, then fell off suddenly to present volume of 
2 1-2 gallons: temperature, 66 degrees; a good drinking water; notice- 
able improvement in the health of those using it. 

Record of J. Manly Foster's well No. 1, Tuscaloosa. 



Feet. 

Sand and gravel — 30 

Blue rock 30 — 80 

Sand and water with occasional streaks of blue 

rock 80 — 234 



No. 2 and 3, bored by Wyndham in the fall of 1904 on Mr. Foster's 
place in Section 22, Township 22, Range 11 W. ; depth, about 250 feet; 
both wells flow good streams from 1 1-4-inch pipe. Nos. 4, 5, and 6, bored 
for Mr. Foster by Wyndham in the spring of 1905, in Sections 13 and 14, 
Township 22, Range 11 W. ; depth, 250-270 feet; all three furnish good 
flow from 1 1-4-inch pipe. 

Well of Will Murphy (colored), in the E. half N. W. quarter of Sec- 
tion 13, Township 22, Range 11 W. ; bored in March ,1905, by Wyndham; 
depth, about 280 feet; weak stream. 

Friedman & Loveman's well, in the N. E. quarter Section 24, Town- 
ship 22, Range 11 W. ; bored by W. V. Morrison in 19(2; depth 320 feet; 
first overflow at 300 feet; 3-inch casing; original volume estimated at 4 
gallons, which gradually increased to present volume, 24 gallons; tempe- 
rature, 06 degrees. 

Record of Friedman & Loveman's well. 



Feet. 

Soil and clay — 30 

Blue rock 30 — 150 

Sand, with thin layers of hard rock 150 — 300 

Hard rock 300 — 320 



A peculiar circumstance is related by Mr. Morrison con- 
cerning this well ; the water first rose to — 5 feet. Three bar- 
rels of water were then poured into the pipe, when the water 
began to flow and has since continued to flow without inter- 
ruption. 

Henry A. Jones's wells, bored by Martin and Morrison in 1902: No. 1, 
on Slade place, in the S. E. quarter S. W. quarter Section 20. Township 
22, Range 10 W. ; depth, 160 feet; principal supply of water at 150 feet; 



120 details: coastal plain division. 

stopped in hard rock; water stands at —7 feet and pump is used. No. 2, 
about 100 yards from No. 1; record practically the same. 

Quarles well, at Poster's Perry bridge; bored by Morrison in 1902; 
depth, 306 feet; 3-inch casing; overflow at 260 feet, weak; since the first 
few days the flow has remained constant at 6 gallons per minute; tem- 
perature, 67 degrees. 

Record of Quarles well, Foster's Ferry. 



Feet. 

Soil and clay — 30 

Blue rock 30 — 150 

Sand and water with an occasional strata of 

blue rock 150 — 306 



EIGHT BANK OF EIVEK. 

Below the above localities, on the right bank of the river, 
there are several wells lately bored, records of which have been 
secured. 

Henry A. Jones's wells, in Sections 5-6, Township 24, Range 53; four 
wells bored by W. V. Morrison in 1902, not more than half a mile apart, 
all flowing, and about the same depth, 166 feet (Morrison) ; No. 1, 3-inch 
casing; flows 70 gallons per minute; temperature, 66 1-2 degrees. No. 2, 
3-inch casing; first overflow at 103 feet; flows, 90 to 100 gallons per minute; 
temperature 66 degrees. No. 3, 4 1-2-inch casing; first overflow at 136 feet; 
present flow, 1 1-2 gallons per minute; temperature 64 degrees. No. 4, 
3-inch casing; first overflow at 136 feet; present volume (estimated), 60 
gallons per minute; temperature, 65 1-2 degrees. 

Guy Poster's well, in Section 7 or S, Township 24, Range 5 E. ; bored 
by Morrison in 1902; depth, 170 feet; equally strong flow at 162 feet; first 
overflow at 130 feet; present volume, 30 gallons per minute; temperature, 
66 degrees. Mr. Poster thinks that heavy rains 50 miles north are fol- 
lowed in three days by an increased volume; otherwise the flow is con- 
stant. Mr. Morrison thinks that all the wells in this neighborhood would 
rise 20 feet above the surface. 

Well of Charles Verner and Henry King, in fraction A, Section 13, 
Township 24, Range 4 E. ; bored by Morrison in 1902; 3-inch casing; depth, 
200 feet; first overflow at 164 feet, somewhat weaker than at 200 feet; 
practically constant volume, 30 gallons per minute; temperature, 67 de- 
grees. 

Record of Verner and King well, near Tuscaloosa. 



Feet. 

Soil, clay — 30 

Blue rock 30 — 150 

Sand with occasional thin strata of blue 

rock 150 — 200 



WATERS OP THE CRETACEOUS. 121 

Henry King's well, 1 mile northwest of the old well at King's Ferry; 
bored by W. M. Martin in 1904; depth, 198 feet; 57 feet of 3-inch casing; es- 
timated flow, 40 gallons per minute. 

HULLS. 

Y. T. Auxford's wells. Hulls station, in Section 17, Township 24, Range 
5 E.; bored by Morrison: No. 1, depth, 234 feet; overflowed at 210 feet; 
3-inch casing; constant volume, 30 gallons per minute; temperature, 07 
degrees. 

Record of Auxford well No. 1, Hulls. 



Feet. 

Soil and clay — 43 

Blue rock 43 — 210 

Sand and water 210 — 234 



The water irom this well has been analyzed by Mr. Hodges, 
with results as shown below: 

Analysis of water from Auxford well No. 1, Hulls. 



Parts per million. 

Potassium (K) 2.4 

Sodium (Na) 4.9 

Magnesium (Mg) 8.4 

Calcium (Ca) 3G.3 

Iron and Alumina (Fe 2 3 ,Al.,0 3 ') 2.5 

Chlorine (CI) 7.0 

Sulphuric acid (S0 4 ) 5.1 

Carbonic acid (HC0 3 ) 148.9 

Silica (SiOj) 17.8 

2::::.:; 



No. 2, 1 mile southwest of Hulls; depth 234 feet; overflow at 200 feet: 
rises 4 feet above the surface; temperature. 66 degrees; volume approx- 
imately constant. No. 3, three-fourth mile southwest of Hulls; depth, 290 
feet; 3-inch casing; overflow at 260 feet; constant volume, 1 gallon; tem- 
perature 66 degrees. 

Record of Auxford well No. 3, Hulls. 



Feet. 

Soil, clay — 30 

Pink sandstone 30 — 200 

Sand, with thin layers of blue rock 200 — 290 



122 details: coastal plain division. 



WILLIFORDS. 



On the right bank of the river, below Thomas Allen's and 
almost on the lower border of the county, is the oldest arte- 
sian well in the county, at Willifords Landing, Plate XIV. 
This well is on the second terrace of the river and is said to 
be 400 feet deep. The water overflows in a stream about an 
inch in diameter, and is quite free from dissolved mineral mat- 
ter. No record can now be obtained of this well, which was 
bored more than fifty years ago. 

Analysis of the water by Mr. Hodges shows the following 
composition : 

Analysis of water from well at Williford's Landing. 



Parts per million. 

Potassium (K) 11.6 

Sodium (Na) 17.4 

Magnesium (Mg) 5.3 

Calcium (Ca) 23.4 

Iron and Alumina (Fe 2 3 , ALO3) 2.5 

Chlorine (CI) 17.4 

Sulphuric acid (S0 4 ) trace 

Carbonic acid (HCO a ) 130.0 

Silica (Si0 2 ) 13.1 

220.7 



BIBB COUNTY. 

Some details' concerning the surface and mineral waters of 
Bibb County have been given above (p. 83) in the section 
on the Coosa Valley Region, Appalachian valleys. The south- 
ern and southwestern parts of the county are occupied by the 
Tuscaloosa sands and clays with their capping of Lafayette, 
and the underground water conditions are entirely similar to 
those in the corresponding parts of Tuscaloosa County. No 
well records from Bibb are available, but it may be asserted 
that the artesian prospects in the lower parts of the county are 
favorable. As in some other counties, the abundance and 
good quality of the surface water afforded by the open wells 
and springs have rendered recourse to artesian borings unnec- 
essary. 



WATERS Ol* Till; CRETACEOUS. 123 

CHILTON COUNTY. 

In this county the general geological conditions are quite 
similar to those in Bibb Comity, and there should be no dif- 
ficulty in obtaining artesian water in the southwestern part, 
where the surface is occupied by the Tuscaloosa formation 
with its Lafayette capping. As' shallow wells, however, gen- 
erally furnish ample supplies of good water, artesian borings 
have not been made in many places, and there are few records.* 

PICKENS COUNTY. 

Surface Features. 

The underlying Cretaceous formations of Pickens County 
are the Tuscaloosa, the Eutaw, and the Selma chalk. The 
Tuscaloosa occupies the northeastern and the Eutaw the south- 
western half of that part of the county lying east of Tombigbee 
River, while the Selma chalk occupies the small area west of 
the river, together with a few scattering tracts along the river 
on the eastern side. 

In the Tnscaloosa-Eutaw territory east of the river the 
county is somewhat broken because of the incoherent character 
of the sands and clays which make up these formations. 
Where the watercourses are not too close together, however, 
the divides between them are level plateaus with the Lafayette 
red-loam soils, underlain by pebbles, which once capped the 
Cretaceous over the entire area. 

Shallow Waters. 

In the relatively small area west of the river, which is' occu- 
pied by the Selma chalk, the Lafayette mantle is in great part 
wanting and the soils are composed of the residual matter from 
the decomposition of the limestone. In this section open wells 
and surface springs are not to be» counted on, because of the 
underlying chalk, bnt in the rest of the county the surface ma- 
terials afford conditions for a fairly adequate supply of water 



*See, however, notice of bored wells near Thorsby — under Appa- 
lachian Division — Talladega Mountain section, p. 67. 



124 details: coastal plain division. 

for springs and wells, though these are liable to be much re- 
duced or to go dry in the summer. On Coal Fire Creek are many 
chalybeate springs and on Lubbub Creek near Reform is a 
noted bold spring which is much visited for health and recre- 
ation. Near the mouth of Lubbub Creek and in the old town 
of Vienna also are bold springs' of pure, cold water. 

Artesian Prospects. 

In the Tuscaloosa and Eutaw formations underlying Pick- 
ens County the alternations of sands and clays and their uni- 
form gentle (southwestward) dip afford favorable conditions 
for artesian systems, borings' for water are usually successful. 
The oldest of these artesian borings were made in the prairie 
or chalk region, or along its eastern border, but recently a few 
wells have been put down in the territory of the older Creta- 
ceous formations, notwithstanding the fact that here a good 
water supply can generally be had from shallow wells and 
springs. 



Wells in the But aw Formation. 

A number of artesian wells have been bored within the terri- 
tory of the Eutaw, chiefly in the vicinity of Bridgeville, on 
Lubbub Creek, along Sipsey River, and near Ringos Bluff and 
Pickensville. Prof. Alexander Winchell has given an account 
of some of these wells in an article in the Proceedings of the 
American Association for the Advancement of Science, 1856. 
The averag-e depth of the wells mentioned in this article is 180 
feet, which would reach the base of the Eutaw or the top of 
the Tus'caloosa as water-bearing sands. As these wells were 
mostly bored before the war, it is impossible at this time to get 
any records of the strata passed through and but few of the 
depth of the borings. Notes have been collected of as many 
as could be heard of, and the temperatures together with the 
volume of water afforded by those visited, are given below. 

The wells near the contact of the Eutaw with the Selma chalk 
would have an estimated depth of 300 feet, more or less, to 
the "fourth water" of the borers, while those near the contact 
of the Eutaw with the Tuscaloosa should be shallower in pro- 



WATERS OF THE CRETACEOUS. 125 

portion to the nearness to the latter. Near this line, however, 
it is probable that water is obtained from the underlying. Tus- 
caloosa sands. 

SIPSEY RIVEB. 

Well on old Doctor Hinton Place, 7 or S miles northeast of Vienna; old 
well; flow (estimated), 5 gallons per minute; temperature, 65 degrees. 

Sipsey Mill well, S miles northeast of Vienna; owned by John Childs; 
flow (estimated), 30 gallons per minute; temperature, 65 degrees. 

Wells on Sam Wilder place; No. I, 9 miles northeast of Vienna; flows 
4 feet above surface; yield, 33 gallons per minute; temperature, 65 degrees. 
No. 2, one quarter mile northeast of old Sipsey Mill and S 1-2 miles north- 
east of Vienna; flows 3 feet above surface; yield, 20 gallons per minute; 
temperature, 65 degrees. 

LUBBUB CREEK. 

From the territory near the mouth of Lubbub Creek and 
for some distance upstream, and in the low ground of Tombig- 
bee River up to Ringos Bluff, the following are reported : 

Old Bridgeville well, on Lubbub Creek, 5 1-2 miles from Vienna; flows 
1 foot above surface, decreasing; i. e. wooden pipe decayed; estimated 
yield, 25 gallons per minute; temperature, 66 degrees. 

ALICEVILLE AND VICINITY. 

At Aliceville, north of Bridgeville, a well now bwned by John Coch- 
rane, has lately been bored by Mr. McGracken; first water at 125 feet; 
stand —19 feet; second water at 180 feet; stand — 16 feet. The record 
down to the depth of 309 feet is as follows: 

Record of Cochrane well, Aliceville. 



Feet. 

Soil and loose materials — 56 

Blue rock 56 — 125 

Sand, water 125 — 130 

Blue rock 130 — 175 

Hard sand 175 — 200 

Blue rock 200 — 240 

Sand, water 240 — 250 

Blue rock 250 — 285 

Sand 285 - 288 

Blue rock 288 — 305 

White clay and black sand 305 — 309 



Wells on Mrs. M. E. Mayhew's place, originally Cunningham place; 
1 1-2 miles southwest of Aliceville; flows 2 feet above surface; yield, 8 
gallons per minute; temperature, 66 degrees. 



126 DETAILS : COASTAL PLAIN DIVISION. 

Aaron Harris's well, 2 miles southwest of Aliceville; flows 4 feet above 
surface; yield, 60 gallons per minute; temperature, 66 degrees. 

Well on McCaa place, 3 miles southwest of Aliceville; estimated flow, 
50 gallons per minute, decreasing, in decay. 

Well on Spruille place, owned by L. E. McKinstry, 4 miles southwest of 
Aliceville; in decay, flow not estimated; temperature, 66 degrees. 

Well on McKinney place, owned by Mrs. L. E. McKinstry, 4 1-2 miles 
southwest of Aliceville; flows 3 feet above surface; estimated yield, 10 
gallons per minute; temperature, 66 degrees. 

Well on Mrs. E. A. McCaa's place, 5 miles southwest of Aliceville; 
flows 1 foot above surface; estimated yield 10 gallons per minute; tempe- 
ture, 66 degrees. 

Well on Billy McCaa place, owned by Gardiner & Somerville; flows 2 
feet above surface; estimated yield 25 to 30 gallons per minute; tempera- 
ture, 66 degrees. 

NEAR TOMBIGBEE KIVER. 

V 

Gardiner & Somerville well, Newport Landing, Tombigbee River; flows 
4 feet above surface; temperature, 67 degrees. 

Well on Nolen place, 4 or 5 miles northeast of Vienna; flow 12 gallons 
per minute; temperature, 66 degrees. 

Well on Dr. Carpenter's place, 4 or 5 miles northeast of Vienna; old 
well; flow 8 gallons per minute, temperature, 66 degrees. 

Well on Dr. Carpenter's place at ferry; old well; yield, 4 gallons per 
minute; temperature, 66 degrees. 

Old well near Baptist Church, 5 miles northeast of Vienna; yield, 1 1-2 
gallons per minute; temperature, 65 1-2 degrees. 

Well on Bonner place, owned by Mr. Hagaman. 5 1-2 miles north of 
Vienna; bored about 1885; flows 1 foot above surface; yield 5 gallons per 
minute; temperature, 65 degrees. 

Well on Gibson place, owned by Mrs. Chapman, 6 miles north of Vi- 
enna; estimated flow, 5 gallons per minute; temperature, 65 1-2 degrees. 

Well on Mayhew place, owned by E. Stewart, 7 miles north of Vienna; 
yield 65 gallons per minute; temperature, 64 1-2 degrees. 

Wells on Gardiner place, 7 1-2 miles north of Vienna: No 1, deepened 
in 1860 to 285 feet; first water at 225 feet, overflowing; second water at 
285 feet, rises 25 feet above surface; estimated volume, 100 to 200 gallons 
per minute; temperature, 65 degrees. There are two other large wells at 
this place which were once used to run a mill: No. 2 has an estimated flow 
of 125 gallons per minute; No. 3, is 300 feet deep. 

G. T. Heard's wells: No. 1, in the N. E. quarter of N. W. quarter Sec- 
tion 20, Township 22, Range 16 W. ; flows 3 feet above surface; yield, 30 
gallons per minute; temperature 66 degrees. No. 2, 8 miles west of Alice- 
ville and 1 1-2 miles southeast of Ringos Bluff, in fractional S. E. quarter 
Section 14, Township 22, Range 17 W. ; on the old Stapp place; estimated 
flow, 50 gallons per minute, decreasing, in decay; temperature, 66 degrees. 

Well on Caraway place, 9 miles west of Aliceville; flows 4 feet above 
surface; estimated yield, 60 gallons per minute; temperature, 67 degrees. 

Bradford well, owned by Abe Gray, 8 miles east of Ringos Bluff; flows 
good strong stream; no details obtained. 

At Ringos Bluff there are 5 old wells, of which some records of 4 
follow: No. 1, at warehouse at bluff; flows 2 feet above surface; yield, 12 
gallons per minute; temperature, 66 degrees. No. 2, 30 yards from No. 
1; estimated flow 40 gallons per minute, decreasing, piping in decay; 



WATERS OF THE CRETACEOUS. 127 

temperature, 66 degrees. No. 3, 100 yards from No. 1; old wooden piping 
decayed to ground, forming a kind of spring; estimated yield 5 gallons 
a minute; temperature, 65 degrees. No. 4, 200 yards east of No. 1; 
flows 2 feet above surface; estimated yield, 4 gallons per minute; tem- 
perature, 65 degrees. 

PICKENSVILLE AND VICINITY. 

Henry Ball's wells: No 1, 5 miles a little west of south of Pickensville, 
in Section 12, Township 22, Range 17 W. ; no details; flows 2 feet above 
surface; yield, 6 gallons per minute; temperature, 65 1-2 degrees. 

Mrs. E. G. Hood's well, 3 miles south of Pickensville; flows 3 feet above 
surface; estimated yield, 7 gallons per minute; temperature, 65 degrees. 

W. R. Rogers's well, 3 miles south of Pickensville, near Jackson 
Ferry; new well, bored by Talley & Cunningham in 1902; depth, 236 feet; 
3-inch casing, 64 feet; flows 2 feet above surface; yield 5 gallons per 
minute; temperature, 63 degrees. 

Record of W. R. Rogers 7 well. 



Feet. 

Sand, gravel, etc — 36 

Blue rock 36 — 42 

Blue mud 42 — 236 



Mrs. W. A. Peterson's well, 2 miles west of south of Pickensville; old 
well; flows 2 feet above surface; yield, 25 gallons per minute; tempera- 
ture, 65 degrees. 

Well on old Walker place, three quarters of a mile south of Pickens- 
ville; yield, 5 gallons per minute; temperature, 66 degrees. 

W. R. Rogers's wells (old): No. 1, half a mile west of Pickensville; 
yield, 75 gallons per minute; temperature, 65 degrees. No. 2, three quar- 
ters of a mile west of Pickensville; flow, 25 gallons per minute, wooden 
pipe in decay; temperature, 64 1-2 degrees. No. 3, three quarters of a 
mile west of Pickensville; flow (estimated), 50 gallons per minute; tem- 
perature, 64 1-2 degrees. 

J. F. Wilkins's wells (old): No. 1, 1 1-4 miles east of Pickensville, on 
Bonner's Mill road on Big Creek; No. 2, 5 miles west of north of Pick- 
ensville; both flowing; no details. 

H. L. Stone's well, on Nance place, 2 1-2 miles northeast of Pickensville, 
a quarter of a mile east of house; old well; no record. 

J. E. Stewart's wells: No. 1, old well, 2 1-2 miles north of Pickensville; 
flowing. No. 2, new well, 2 1-2 miles northwest of Pickensville; bored by 
Talley & Cunningham; depth, 260 feet; 3-inch casing, 22 feet; flows 2 1-2 feet 
above surface; yield, 8 gallons per minute; somewhat stronger than the 
new well of W. R. Rogers above mentioned. 

Well on Lee place, in Lees Bend, 6 miles northwest of Pickensville; 
owned by J. E. Stewart, 1 mile northwest of his well No. 2 above men- 
tioned; flowing: not visited. 



128 details: coastal plain division. 

Wells in the Selma Chalk. 

VIENNA AND VICINITY. 

The "rotten limestone" or Selma chalk makes the surface 
only in that part of the county west of the Tombigbee, with the 
exception of a small tract near the mouth of Sipsey River, about 
the town of Vienna. Most of the wells in this section, as in 
the territory of the Eutaw formation, were bored many years 
ago, before the civil war, and the records have been lost. In 
the article above referred to Professor Winchell, on the au- 
thority of Mr. James Strait, a well borer, formerly of Greene 
County, gives the depths of the artesian wells at and near 
Vienna as from 350 to 400 feet. This depth would reach the 
"fourth water" of Mr. Hawk (see p. 113), and it is probable 
that the majority of the flowing wells of the prairie region are 
supplied by these strata near the base of the Eutaw formation. 

The following partial records' of some of the wells have been 
obtained : 

W. B. Peebles wells, in the S. B. quarter S. W. quarter Section 34, 
Township 24, Range 2 W.: No. 1, depth, about 350 feet; flow, 3 gallons 
per minute; temperature, 66 degrees. No. 2, yield, 1 1-2 gallons per min- 
ute; temperature, 66 degrees. No. 3, old well; flows 2 gallons per minute; 
temperature, 66 degrees. No. 4, bored about 1885; depth about 380 feet; 
flow, 3 gallons per minute; temperature, 67 degrees 

Mrs. Sallie Turnipseed's well, locality same as above; old well, in Vien- 
na; no record. 

Well on old Wyndham place, one" mile northeast of Vienna, owned by 
W. B. Peebles; flow, 30 gallons per minute; temperature, 67 degrees. 

Gold Dust farm well, 1 or 2 miles northeast of Vienna, owned by Mr. 
Hagaman, of Vienna; flow, (estimated), 5 gallons per minute, piping in de- 
cay, so that it forms a kind of spring. 

Well on Wilder place; 1 or 2 miles northeast of Vienna; old well; flows 
5 gallons per minute; temperature, 66 degrees. 

Well on Ferguson place, near Vienna; old well; flow, half a gallon per 
minute; temperature, 66 degrees. 

Well on Cherry place, near Vienna; old well; flow, 2 gallons per minute; 
temperature, 66 degrees. 

Well on Manning place, near Vienna, owned by Mr. Hagaman; flow, 
1 1-2 gallons per minute; temperature, 66 degrees. 

Well on Wilder place, owned by W. B. Peebles; piping in decay, no 
record. 

Wells on Richardson place, 2 or 3 miles northeast of Vienna, owned by 
Mr. "Hagaman; bored long before the war by Mr. Garrow, to furnish 
water for a mill; all close together: No. 1, flows from a 6-inch pipe at 
the level of the ground; estimated flow, 50 to 75 gallons per minute; tem- 
perature, 66 degrees. No. 2, estimated flow, 10 to 15 gallons per minute; 
temperature 66 1-2 degrees. No. 3, water flows from a 6-inch pipe at the 



WATERS OF THE CRETACEOUS. J k 29 

bottom of a gulch, 10 feet below the surface; estimated flow, 50 to 75 
gallons per minute. No. 4, water flows from an S-inch pipe (cypress log), 
in gulch S feet below surface of ground; estimated How, 75 to 100 gallons 
per minute; temperature 66 degrees. No. 5, flows at surface; estimated 
yield, 6 gallons per minute; temperature. 66 degrees. 

Wells on Barnes place, 2 or 3 miles northeast of Vienna, owned by 
Peebles & Hagaman. One well flows 3 feet above the surface; estimated 
yield, 30 gallons per minute; temperature, 66 degrees. Two other wells on 
tliis place have about the same flow and temperature. 

Hagaman wells, in the S. W. quarter of N. E. quarter Section 27, 
Township 24. Range 2 W.: No. 1 Mows 12 gallons per minute; tempera- 
ture 66 degrees. No. 2, hows 1 gallon per minute; temperature. 66 de- 
grees. 

STONE AND VICINITY. 

West of Tombigbee river, at Stone and vicinity and farther 
west, there are many old wells of which the records are not now 
obtainable, but concerning which a few notes may be present- 
ed, and several new wells have been bored which supply addi- 
tional needed information. 

Public well, Stone, old well; water formerly overflowed but now stands 
at —2 feet; estimated volume, 3 or 4 gallons per minute; temperature, 
68 degrees. 

Dr. B. T. Jones's well, 200 yards east of post-office in Stone; new well, 
bored by C. T. White in 1902; depth 400 feet; 3 1-2-inch casing, 22 feet; 
2-inch casing, 300 feet; first water at 150 feet; second water at 200 feet; 
third water at 400 feet; water rises 4 feet above surface; yields, 2 1-2 
gallons per minute; temperature, 67 degrees. The record is as follows: 
Soil, clay, etc., — 22 feet; blue rock, 22 — 100 feet; sand and gravel, 
with occasional rock, 100 to 400 feet. 

Dr. T. H. G. Cook's well, Stone; new well; bored in 1902 by C. T. 
White; depth, 650 feet; 2-inch casing, 600 feet; first water at 250 feet, 
stand —7 feet; second water at 300 feet, stand —7 feet; third water at 
560 feet, rising to surface; excavated 3 feet to get overflow. 

Walter Wyndham's wells, a half mile west of Stone: No. 1, flows 1 1-2 
gallons per minute; temperature, 67 degrees. No. 2, formerly overflowed; 
stand now —10 feet; has been sounded to the depth of 300 feet. 

R. C. Long's well, three quarters mile east of Stone, at ferry; flows 
3 feet above surface; yield, 1 1-2 gallons per minute; temperature, 67 de- 
grees. 

J. B. Somerville's well, 1 1-2 miles east of Stone; new well; bored by 
White in 1902; depth, 500 feet; 4-inch and 2-inch casing to bottom; first 
water at 400 feet; formerly overflowed, but water stands now just at 
surface. On the same place are several old wells, most of them no lon- 
ger flowing: No. 1, 150 yards south of house; overflows in the winter 
only. No. 2. formerly overflowed; water stands now at —4 feet. No. 3, 
one mile east of house; flows 4 feet above surface, a good stream. 

On the Winston Jones and Goldsby places, 3 miles west of Stone, are 
several old flowing wells. 
9 



130 DETAILS : COASTAL PLAIN DIVISION. 

SHERMAN,* DANCY AND VICINITY. 

In the lower edge of Pickens County, about Sherman and 
Dancy are several wells of which the following records are 
available : 

T. Moore's well, 1 mile south "of Sherman, in Section 14, Township 23, 
Range 3 W. ; old well; bored about 1870 by Joe Ladd (colored); depth, 600 
feet; diameter, 4 inches; flow, 6 1-2 gallons per minute; temperature, 72 
degrees. 

Will Oliver's well, 1 mile west of Sherman; old well; flow, I 1-2 gallons 
per minute; temperature, 70°. 

Well of Mrs. Adams, 2 miles west of Sherman; bored about 1870 by 
Mi. Ladd; depth, 602 feet; flow, 30 gallons per minute; temperature, 72 1-2°. 

W. B. Whittens well, 3 miles west of Sherman; bored by Bicksler in 
1900 or 1901; depth, 725 feet; temperature, 71°. 

Wells of Mrs. Peter Wier, Sr., 3 miles west of Sherman; three old wells, 
bored about 1860. One of these yields 2 1-2 gallons per minute, tempera- 
ture, 71°. The other two are now in decay. 

Well on King place, 3 3-4 miles west of Sherman; very old, and with 
very small stream; no record. 

T. A. Baker's wells, Dancy; No. 1, bored by White in 1899; depth, 700 feet; 
not flowing; first water at 450 feet; second water, at 600 feet, stand -8 
feet; third water at 700 feet, stand -22 feet. Record: Soil, 0-15 feet; blue' 
rock, 15-280 feet, quicksand, 2S0-320 feet; sand and thin rods, 320-600 feet. 
No. 2, bored by Ladd; depth, 450 feet; water stands at -10 feet; steam 
pumping for twenty-four hours does not lower level. No. 3, abandoned; 
record same as No. 2. 

J. H. McDonald's well, 2 1-2 miles north of Dancy; bored by White in 
June, 1903; depth, 350 feet; diameter, 3 1-2 inches; water stands at -90 
feet; pumped. The ground level here is estimated to be 75 feet above 
Dancy. Record: Soil, 0-20 feet; blue rock, 20-300 feet; sand and rock, 
300-350 feet. 

W. D. King's well, 2 miles west of Dancy; bored by Bicksler in 1901; 
depth, 903 feet; cased 797 feet; first overflow at 903 feet; 3 1-2 gallons per 
minute; stand -20 feet. Record: Soil 0-21 feet; blue rock, 21-361 feet; sand 
and rock, 361-800 feet; hard rock, 800-903 feet. 



* Sherman is near the line of Pickens County but is in reality in 
Sumter county. The Moore, Oliver and Weir wells are in Sumter 
county; the others mentioned are in Pickens. 



WATERS OF Tin; CRETACEOUS. 131 

SUMTER COUNTY. 

SURFACE IEATURES. 

The dividing- line between the Cretaceous and Tertiary beds 
in Sumter Count}- pass'es in a northwest-southeast direction 
through Livingston, the county seat. The Cretaceous strata 
are for the most part Selma chalk, with a narrow belt of the 
Ripley formation along the south'ern border. Southwest of the 
Cretaceous beds are the Tertiary strata of the Midway and 
Black Bluff, or Sucarnochee (post-oak Flatwoods) formations, 
extending as far as York station, beyond which the other beds' 
of the lower Tertiary make the surface of the county to its 
southwestern limit. 

Topographically, that part of the county occupied by the 
Cretaceous strata is in general gently rolling rather than hilly ; 
but through Sumterville and on to a little west of Epes runs a 
prominent ridge which owes its existence to a slight difference 
in the quality of the limestone rock. The town of Sumterville 
is situated on this ridge, and from its summit one may overlook 
the country from Tombigbee River on the one side to the Miss- 
issippi line and beyond on the other. This ridge and the de- 
pression of the Flatwoods are the two most pronounced topo- 
graphic features of the county. Another prominent ridge, 
based on what is' commonly known as "horse-bone rock", passes 
northwestward through Warsaw and Sherman, in the extreme 
northern part of the county. Between this ridge and that on 
which Sumterville stands the limestone is quite pure and uni- 
form in quality, and makes the most fertile and attractive of 
the farming lands. In this belt are found most of the artesian 
wells of the county, since the Sumterville ridge is in general 
too high for flowing wells', and south and west of it the wells 
would as a rule be too deep for economy. 

Shallow Waters. 

Springs in the Selma Chalk. 

NEAR EPES. 

As may be inferred there is a general scarcity of surface 
springs in the chalk region of Sumter County, but there is one 
never failing spring in the southeast corner of the S. W. quar- 



132 details: coastal plain division. 

ter S. E. quarter, Section 6, Township 19, Range iW. ; about 
7 miles northeast of Livingston, 3 miles southeast of Epes, and 
2 miles from Tombigbee River, on the plantation of Mr. Har- 
den L. Jones, of Livingston. The water oozes from a fissure 
in the chalk rock, here slightly fossiliferous, and collects in a 
shallow pool. As it was' thought to have medicinal properties, 
it has been analyzed by Mr. Hodges, with the result given 
below : 

Analysis of water from H. L. Jones's spring, near Epes. 



Parts per million. 

Potassium (K) 14.6 

Sodium (Na) 374.2 

Magnesium (Mg) 277.7 

Calcium (Ca) 617.7 

Iron (Fe) trace 

Chlorine (CI) 665.5 

Sulphuric acid (S0 4 ) 2089.0 

Carbonic acid CHC0 3 ) 453.8 

Silica (Si0 2 ) 14.5 

4507.0 



Springs in the Tertiary Formations. 

In the Tertiary formations of Sumter County there is gen- 
erally no lack of fairly good surface waters, except in the belt 
of post-oak Flatwoods, underlain by the black Sucarnochee 
clays which weather to a reddish color. This whole belt is only 
slightly elevated above the general drainage plain, and is com- 
paratively level, as the name indicates. After rains the water 
stands in all the slight depressions, or runs off into streams, 
and very little of it soaks into the clay. As a consequence, no 
supply of surface waters for wells can be depended on. Cis- 
terns dug into the solid clay and filled with rain water from 
the house tops supply domestic needs', and shallow ponds are 
utilized for cattle. 

In some parts of this region shallow wells find a meagre sup- 
ply of water in the clay, but it is' apt to be highly impregnated 
with salts of various kinds and is unsuitable for drinking- ex- 
cept by those accustomed to it. 



WATERS OK THE CRETACEOUS. 133 



YORK AM) VICINITY. 



On the plantation of Mr. W. A. Altnian, about i 1-2 miles 
south of York on the Butler road is a well the water of which 
is used by the negroes on the place, who claim to be fond of it, 
though they say they cannot drink much of it because of its' 
weakening effect, due no doubt to die Epsom salts with which 
it is strongly impregnated. An analysis of this water by Air. 
Hodges shows the following composition : 

Analysis of water from* Altman well, near York. 



Parts per million. 

Potassium (K) 37.3 

Sodium (Na) 705.1 

Magnesium (Mgj 726.1 

Calcium (Ca) 501.3 

Iron and alumina (Fe»0 3) AU0 3 ) 16.9 

Chlorine (CI) 461.1' 

Sulphuric acid (SO.,) 4636.2 

Carbonic acid (HC0 3 ) 404.5 

Silica (Si0 2 ) 75.8 

7564.4 



Two, and perhaps more, wells in York have water somewhat 
similar in composition, though not so strongly saturated, as 
may be seen from the analysis given below : 

A7ialysis of water from C. B. Mill's well, York. 



Parts per million. 

Potassium (K) 61.9 

Sodium (Na) 359.8 

Lithium (Li) trace 

Magnesium (Mg) 542.4 

Calcium (Ca) 530.3 

Iron and alumina (Pe 2 3 , Al 2 O a ) 17.0 

Chlorine (CD 460.8 

Sulphuric acid (S0 4 ) 3553.4 

Carbonic acid (HCO a ) SO. 3 

Silica (Si0 2 ) 55.0 

5660.9 



134 DETAILS: COASTAL PLAIN DIVISION. 

. Analysis of water from, Dr. R. H. Hale's well, York. 



Parts per million. 

Potassium (K) 14.1 

Sodium (Na) 379.1 

Magnesium (Mg) 258.6 

Calcium (Ca) 315.3 

Iron (Fe) 86.6 

Chlorine (CI) 354.5 

Sulphuric acid (S0 4 ) 2283.3 

Silica (Si0 2 ) 92.4 

3783.9 



At Curl station on the Southern Railway, a short distance 
•east of York, a well has been sunk in the Flatwoods clays, and 
the water has a composition similar to the above, as may be 
seen from Mr. Hodges'^ analysis : 

Analysis of water from B. HigMower's well, Curl station. 



Parts per million- 
Potassium (K) 22.5 

Sodium (Na) 540.2 

Lithium (Li) trace 

Magnesium (Mg) 383.8 

Calcium (Ca) 607.2 

Iron and alumina (Fe 2 3 , A1 2 3 ) 18.2 

Chlorine (CI) 761.1 

Sulphuric acid (S0 4 ) 3085.0 

Carbonic acid (HC0 3 ) 14.0 

Silica (Si0 2 ) 42.9 

5474.9 



The waters of the flatwoods will be referred to again under 
Marengo County. 

The Cretaceous and Tertiary formations in Sumter and other 
counties' of the Coastal Plain are mantled by pebbles and red 
loam of the Lafayette formation, and where erosion has re- 
moved least from the surface, as on the divides, the lands are 
almost level and are capped by this red loam with the pebbles 
below it. In these table-lands there is an ample supply of the 
best freestone water, gathered and stored in the sands and 
pebble beds'. Wherever these conditions prevail no borings for 
artesian waters have generally been made. In the territory of 



WATERS OF THE CRETACEOUS. 135 

the Selma chalk the remnants of the red loam and pebble beds 
are generally small and insufficient to provide a durable water 
supply. In the sandier parts of the Cretaceous (Ripley) and in 
the greater part of the territory south of the Flatwoods the 
Lafayette mantle remains in good part intact, and the water 
supply is correspondingly adequate for open wells and springs. 

Artesian Prospects. 

The records' presented below show fairly well the artesian 
conditions in Sumter County. They are given in the approxi- 
mate order of their geographic and geologic relations ; the 
wells in Warsaw and vicinity being in the northern part of 
the county and nearest the base of the Selma chalk, and the 
others following progressively southward and westward and 
being on successively later strata* 

The deep wells all derive their water from the Eutaw sands. 

WARSAW AND VICINITY. 

Town well No. 1, located in street: bored in 1848 by Feter Burns; depth, 
400 (?) feet, diameter, 4 inches; first overflow at 300 feet; well originally 
flowed a 2-inch stream; on sounding the well in 1S93 Peter Clements 
found it to be only 300 feet deep; present flow, 1 1-2 gallons per minute. 

Town well No. 2, in street, 150 yards northwest of No. 1; bored by Peter 
Burns in 1S49; depth, 450 feet; diameter, 4 inches; first flowing water from 
300 feet; yield two-thirds gallons per minute; stands 1 foot below the 
surface. 

J. W. Gentry's well, bored by C. T. White in 1900; depth, 560 feet; casing, 
26 feet of 3-inch pipe; first water at 300 feet, rose 10 feet above the sur- 
face; second water at 560 feet, rose 40 feet above the surface; original 
flow (estimated), 250 gallons per minute; present flow, 5 1-2 gallons per 
minute; temperature, 71°. 

Mrs. J. W. Bell's well, near Warsaw, in Section 33, Township 23, Range 
2 W. ; bored in 1851 by Peter Burns; depth, 400 feet; original flow, 1 1-2 
inch stream from depth of 300 feet; present volume, 1 gallon per minute; 
temperature. 68°. 

Well on old N. A. Rogers place, in Section §3, Township 23, Range 2 W., 
near Warsaw; bored by Peter Burns in 1850; depth, 450 feet; flow, froro 
300 feet; now in decay. 



*Some of the wells in the vicinity of Sherman are in Sumter 
County, though described under Pickens County. Sherman is very 
close t® t^e county line, but in Sumter. 



136 DETAILS: COASTAL PLAIN DIVISION. 

Well on Rogers estate, near Warsaw; "bored by Simon & Ladd in 1897; 
depth, 300 feet; diameter, 4 inches; first flow at 250 feet; volume, 1 1-2 
gallons per minute; temperature, 68°. 

Well on Weston place, near Warsaw (?); depth, 396 feet; flows one- 
third of a gallon per minute; temperature, 69°. 

Well on J. J. Little's estate, one-half mile north of Warsaw; bored be- 
tween 1S50-1S60 by John Horn; 1 1-2 inch stream originally, but now yields 
one-quarter of a gallon per minute; temperature, 70°. 

William "Willis's well, 1 1-2 miles north of Warsaw; bored about 1850 by 
John Horn; no record. 

J. J. Little's well, on Washington place, 4 miles north of Warsaw; no 
data obtainable. 

Wiley Barnes's well, 2 1--2 miles north of Warsaw; bored in 1847; origi- 
nally gave a 2-inch stream. 

Robert Oliver's well, 4 miles north of Warsaw; new well; flow, 5 gallons 
per minute; temperature, 70°. 

Wells en Andrew Lyon's place, 4 1-2 miles north of Warsaw; No. 1, 
bored in 1855 (?); water stands at -60 feet. No. 2, 40 feet lower than No. 
1; flows, 10 gallons per minute; temperature, 09°. 

J. P. Rogers's well, one half mile northwest of Warsaw; bored in 1847 
by Peter Burns; originally gave a 1 1-2 inch stream, but was abandoned 
thirty years ago. 

Well on Nan Stone place, 1 1-2 miles northwest of Warsaw; bored about 
1845; original stream, 1 1-2 inch; present volume, one-half gallon per min- 
ute; temperature, 69°. 

William Peebles's well, 2 miles northeast of Warsaw: bored in 1S45 by 
John Horn; originally gave 2 1-2 to 3 inch stream. 

Well on old Bell place, 3 miles northwest of Warsaw; water stands at 
-18 feet. 

C. J. Brockway's well, 4 miles northwest of Warsaw; bored by Ladd m 
189S; flow, 2 gallons per minute; temperature, 72°. 

J. P. Rogers's well, one-fourth mile west of Warsaw, in Section 33, 
Township 23, Range 2, W. ; bored by C. T. White, in 1901; depth, 300 feet; 
cased to rock with 3-inch casing; first water at 220 feet, rising 10 feet 
above surface; original volume, 6 gallons per minute; temperature 69°. 
Record; Sand, 0-26 feet; blue rock, 26-220 feet; sand and water, 220-300 feet. 

P. M. Grove's well, one-half mile west of post office at Warsaw, in Sec- 
tion 33, Township 23, Range 2 W.; bored by C. T. White in 1901; depth, 
460 feet; casing, 20 feet of 3 1-2 inch pipe; first water at 250 feet, rose to 
-10 feet; second water at 300 feet, rose to -10 feet; third water at 40Q 
feet, overflowing; fourth water at 460 feet, flows; yield, 1 gallon per 
minute; temperature, 70°; water found beneath a thin, solidified layer. 

Well of Oliver & Oliver, 8 miles west of Warsaw; small stream. 

Well on Mac Roger's place, 5 miles southwest of Warsaw; old well; 
flows 1 1-4 gallons per minute; temperature, 69°. 



WATERS OL' THK CRETACEOUS. 137 

J. I r. Vinson's wells, 7 miles southwest of Warsaw, in Section 9; Town- 
ship 21'. Range 3 W. ; No. 1 bored by J. \V. Patterson in 1902; depth, 702 
feet; easing, 250 feet of 2-inch pipe, 4-inch casing at top; supply, from 
the third water horizon, will rise to 40 feet above surface; flow, 2 gallons 
per minute; temperature, 71°. No. 2, bored about 1855; flows, one-third 
of a gallon per minute; temperature, 68°. 

J. W. Patterson's well, 7 miles southwest of Warsaw, in Section 23, 
Township 22, Range 3 W.; bored by C. T. White, in 1901; depth. 700 feet; 
casing, 3 1-2 inch to rock; 250 feet of 2-inch pipe; first water at 400 feet, 
rose to -30 feet; second water at 500 feet, rose to -30 feet; third water at 
700 feet, rose to 6 feet above surface; estimated flow, 1 to 2 gallons per 
minute. 

Record of Patterson ivell, 7 miles southwest of Warsaw. 



Feet. 

Soil — 20 

Blue rock 20 — 200 

Hard, dry sand 200 — 300 

Blue rock 300 — 460 

Sand 460 — 500 

Soapstone 500 — 700 



Well on Taylor place, 2 miles south of Warsaw in Section 9, Township 
22, Range 2 W.; bored about 1855 by John Horn; depth, 400 feet; cased be- 
low rock with iron pipe; good stream until 1902, when it was stopped by 
entrance of sand. 

GAINESVILLE AND VICINITY. 

Some distance down the river, about Gainesville, artesian 
wells are numerous, many of them dating back to before the 
civil war. In general the first water in the vicinity of Gaines- 
ville is much more salty than the second. The following are 
the records : 

John Rogers's well, Gainesville; depth, 630 feet; principal water supply 
at 630 feet; water rises to 20 feet above surface; quality good; well starts 
in the "rotten limestone" and obtains its supply from the Eutaw forma- 
tion; blue rock is reached at 27 feet from the surface and is 383 feet thick. 

Old mill well, Gainesville; owned by the town; bored about 1850; depth, 
600 feet; formerly overflowed, but is now rumped; yield, 1 1-2 gallons per 
minute; temperature, 09°. 

R. H. Long's well, near Gainesville, in Section 2, Township 21, Range 2 
W., bored by C. T. White in 1900; depth, 626 feet, rose to 25 feet above the 



138 details: coastal plain division. 

surface; estimated flow, 10 gallons per minute; no decrease. Record: Gravel 
and sand, 0-43 feet; blue rock, 43-375 feet; sand and water, 375-475 feet; 
"soapstone," 475-626 feet. 

John A. Rogers's well, near Gainesville in Section 7, Township 21, Range 
2 W. ; bored by C. T. White in 1900; depth, 630 feet; casing, 300 feet of 
2-inch pipe; first water, at 375 feet, rose to -24 feet; second water, at 630 
feet, rose to 20 feet above the surface; flow, 5 gallons per minute; volume 
constant; temperature, 73°. Record: Soil, 0-20 feet; blue rock, 20-375 feet; 
sand and water, 375-475 feet; "soapstone," 475-630 feet. 

Mrs. Ben Moy's well, 4 miles north of Gainesville; old well; flow very 
weak, decreasing, in decay. 

Mrs. Mooring's well, 5 miles north of Gainesville; bored by Joe Ladd 
(colored) in 1875 (?); flow, 1 gallon per minute; temperature, 71°; 4 inch 
casing to blue rock. 

Well on Sallie Rogers's place, 6 miles north of Gainesville; bored by C. 
T. White in 1899; depth, 500 feet; casing, 30 feet of 3 inch pipe; estimated 
original volume 15 gallons; flow now 1 1-3 gallons per minute; tempera- 
ture, 71°; first water, at 350 feet, rose just to surface; second water, at 
450 feet, rose to 30 feet above the surface. Record: Soil, 0-20 feet; blue 
rock, 20-350 feet. 

Mrs. L. A. Landford's old well, 2 miles northwest of Gainesville; flows 
one-eighth of a gallon per minute, at 4 feet above the surface; tempera- 
ture, 69°. 

L. A. Knight's well, 6 miles northwest of Gainesville; bored by Howard 
Horn in 1855 (?) ;flows 1 1-4 gallons per minute; considerable leakage; 
temperature, 69°. 

Well on Marsh place, 7 1-2 miles northwest of Gainesville; old well, 
yielding 1 1-2 gallons per minute; temperature, 70°. 

Long & Patterson wells, in Section 4, Township 21, Range 2 W. : No. 1, 
1 1-2 miles west of Gainesville; bored by C. T. White in 1900; water stands 
at -1 foot; depth, 700 feet; casing, 25CT feet of 2-inch pipe; temperature, 
69°; first water, at 475 feet, rose to -40 feet; second water, at 700 feet, 
rose to -15 feet. Record: Blue rock, 0-475 feet; sand and water, 475-515 
feet; successive strata of blue rock and clay, 515-700 feet. No. 2, 1 3-4 miles 
west of Gainesville; bored by C. T. White in 1900; depth, 700 feet; casing, 
250 feet of 2-inch pipe; estimated to be 12 feet lower than No. 1; original 
flow, about 6 gallons per minute; present flow, 2 gallons per minute; tem- 
perature, 74°. No. 3, 1 1-2 miles west of Gainesville; bored by J. W. Pat- 
terson in 1902; depth, 676 feet; water rising to 30 feet above the surface 
at 676 feet; flow, stopped by accident; water now stands at -15 feet. 

Well of "William Wier (colored), 4 miles southwest of Gainesville; bored 
by C. T. White in 1900; depth, 700 feet; casing, 200 feet of 2-inch pipe; first 
water, at 500 feet, rose to -5 feet; second water, at 700 feet, rose to 20 
feet above the surface (?); original volume estimated at 15 gallons per 
minute; present volume, 1 gallon per minute; temperature. 71°. Record: 
Soil, 0-20 feet; blue rock, 20-500 feet; sand and water, 500-550 feet; soap- 
stone, 550-700 feet. 



WATERS OE THE CRETACEOUS. 139 

Sam T. Jones's wells: No. 1, on Wyndham place, 3 1-2 miles south of 
Gainesville; flows, one-quarter of a gallon per minute, formerly much 
stronger; temperature. 71°. No. 2, 2 1-2 miles south of Gainesville; borefi 
by C. T. White in 1901; depth, 700 feet; original flow, 12 gallons per minute; 
present flow, about one-half gallon per minute; temperature, 70°; first 
water, at 400 feet, rose to -20 feet; second water, at 475 feet, rose to -20 
feet; third water, at 700 feet, rose to 17 feet above the surface. Record: 
Soil, 0-20 feet; blue rock, 200-400 feet; sand, 400-450 fet; clay, 450-475 feet; 
sand and water, 475-700 feet. No. 3, one-half mile south of Gainesville; 
bored by J. Ladd to 3G0 feet, and finished to 700 feet by C. T. White in 
1901; water formerly flowed, but now stands at -1 foot; casing 20 feet of 
5-inch pipe; a flow of water, rising to -20 feet, was encountered at 432 
feet. Record from 360 feet: Sand and water, 360-400 feet; successive strata 
of sand and soapstone, 400-700 feet. 

T. L. Smith's well, 2 miles south of Gainesville; bored by C. T. White in 
1901; depth, 735 feet, casing, 320 feet of 3 1-2 and 2-inch pipe; original flow, 
1 or 2 gallons per minute. Record: Soil, 0-20 feet; blue rock, 20-400; pene- 
trated four strata of sand. 

Well of Tom Minneice (colored), 3 1-2 miles south of Gainesville in Sec- 
tion 18, Township 21, Range 1 W.; bored by C. T. White in 1900; depth, 
600 feet; easing 300 feet; original volume (estimated), 25 gallons per minute; 
present volume, 12 gallons per minute; first water at 300 feet, rose to 10 
feet above the surface; second water, at 600 feet, rose to 25 feet above 
the surface; temperature, 71°. Record: Soil (clay), 0-34 feet; blue rock, 
34-276 feet; sand and water; 276-600 feet. 

R. H. Long's well, 2 1-2 miles southeast of Gainesville, in Section 13, 
Township 21, Range 2 W.; bored by C. T. White in 1900; depth, 600 feet; 
casing 250 feet of 2-inch pipe; first water at 350 feet, rose to -20 feet; second 
water, at GOO feet, rose to 20 feet above the surface; original flow, 15 gal- 
lons per minute; present flow, 3 gallons per minute; temperature, 72°. Rec- 
ord: Soil, 0-20 feet; blue rock, 20-350 feet; sand, 350-400 feet; soapstone, 
400-600 feet. 

Well on Senator Morgan place, 4 miles southeast of Gainesville, in Sec- 
tion IS, Township 21, Range 1 W.; deepened from 350 to 550 feet by C. T. 
White; flow, 3 3-4 gallons per minute at 4 feet above the surface; no de- 
crease since well was deepened; temperature, 71°. 

J. A. Rogers's old wells on Swilley place: No. 1, 5 miles southeast of 
Gainesville, in Section 20, Township 21, Range 1 W. ; water formerly 
flowed, but now standi at -8 feet. No. 2, 6 1-2 miles southeast of Gaines- 
ville, in Section 22, Township 21, Range 1, W.; flow, 7 gallons per minute at 
3 feet above the surface; temperature, 69°. 

EPES AND VICINITY. 

Well of Epes Cotton Oil Company, at Epes, on the right bank 
of the Tombigbee, on Jones Bluff, the site of old Fort Consti- 



140 DETAILS : COASTAL PLAIN DIVISION. 

tution ; bored in 1899 by J. I. Hawk. The altitude of Epes is 
125 feet and it stands on the white chalk rock. Depth of well, 
737 feet; record as follows: 

Record of Epes well. 



Feet, in. 

Blue rock 442 6 

Reddish muddy substance 65 

Greenish sand, with water 103 

Stone 8 

Rusty, hard pan 70 

Stone 3 

White sand 42 



At first a small stream ran out at the surface; on lowering 
the boring', a rather better stream was obtained, but it is still 
weak, less than a gallon a minute ; surface about the well has 
been lowered in order to get better overflow. An analysis of 
this water was furnished by Mr. W. B. Harkness',* who also 
furnished the record of the well : 

Partial analysis of water from Epes well. 



Parts per million. 

Total solids in solution 3605.26 

Volatile and organic 60.24 

Chlorine (CI) 1927.13 

Iron and alumina (Fe 2 3 , ALO.O 3.94 

Silica (Si0 2 ) 11.81 

Magnesium (Mg) 14.95 

Calcium (Ca) 45.17 

Sulphuric acid ,S0 4 ) Trace 

Sodium (Na), present in large amount taut not 

determined 
Carbonic acid, present but not determined. 
Potassium (K) Trace 



Mrs. A. M. Tart's well, 3 miles southeast of Epes; bored by Murray 
about 1852; depth, 930 feet; cased 400 feet; flowing water between 800 and 
900 feet; yield, 28 gallons per minute; temperature, 79°. 

W. A. C. Jones' well, 1 1-4 miles southwest of Mrs. Tart's well above 
mentioned, but about 150 feet higher on a hard limestone ridge. Bored by 
E. L. Machamer, 1906. Depth, about 1,000 feet. Water rises to within 
100 feet of surface, pumped by windmill. Casing at bottom 150 feet 2-inch 
pipe, and on this 160 feet of 2 1-2 inch pipe. 

*Bxpressed by analyst in grains per gallon; recomputed to parts 
per million at U. S. Geological Survey. 



WATERS OF THE CRETACEOUS. 141 

Record of W. A. C. Jones' well. 



Feet. 

Brownish soft top soil 1» 20 

Blue rotten lime rock 20 — 72 

White soft lime rock 72 — 495 

Tough white rock 495 — 571 

Blue lime rock 571 — 7(57 

Hard white sand rock 767 — 773 

Greensand with water 773 — 778 

Fine sand rock with thin layers of hard rock 
and water which rose to within 1 Lis feet 

of top 778 — 834 

"Very hard blue flint rock 834 — 836 

Greenish sand with water 836 — 870 

Soft, dark and muddy earth alternating with 

beds of hard rock and sand, water bearing.. 870 — 992 



T. V. White's well, 3 l-2_miles northwest of Epes, in Section 11, Town- 
ship 20, Range 2 W.; bored by C. T. White in 1901; depth, 700 feet; original 
flow, 3 gallons per minute; temperature, 72°; first water at 500 feet; rose 
to -3 feet; second water, at 550 feet, rose to -15 feet; third water, at 700 
feet; flows; casing, 320 feet. Record: Blue rock, 0-500 feet; sand with 
water, 500-540 feet; clay, 540-550 feet; sand with water, 550-570 feet; pink 
soapstone, 570-700 feet. 

Louis Brown's well, 5 miles northwest of Epes, in Section 9, Township 
20, Range 2 W. ; bored by C. T. White in 1901; depth, 735-feet; water level, 
-15 feet; first water, at 600 feet, rose to -40 feet; second water, at 650 feet, 
rose to -40 feet; third water, at 735 feet, rose to -15 feet; temperature 72°. 
Blue rock, 600 feet thick; otherwise, record is similar to that of T. V. 
White's well. 

SUMTERVILLE AND VICINITY. 

The elevation of the ridge on which Sumterville stands is 
too great for flowing water, but by artesian borings water could 
certainly be obtained sufficiently near the surface to be raised 
by pumps. At present the water supply is obtained from cis- 
terns'. At the base of the ridge, with proper selection of local- 
ity, flowing water might be obtained, but the boring would be 
deep, as is shown by the records at Epes and Livingston. 

LIVINGSTON AND VICINITY. 

On the upper strata of the chalk formation and the overly- 
ing Ripley stands Livingston, the county seat of Sumter 
County. Here a well has been bored which exhibits the full 
thickness of the chalk. The record is as follows: Soil and 



142 details: coastal plain division. 

surface sands, 20 feet; Selma chalk, or blue rock, 930 feet; 
Eutaw sands to bottom of well (1062 feet), 112 feet. The 
first water was reached immediately below the blue rock, at 966 
feet, affording a small stream which rose to the surface; at 
1005 feet a larger stream was obtained in coarse green sand, 
and deeper drilling discovered no other water. The flow is 
quite feeble, the water barely reaching the surface, which has 
been lowered about the mouth of the well for convenience 
in collecting the water. 

Analysis of water from well at Livingston. 
Analyst, Dr. R. E. Webb* 



Parts per million. 

Sodium (Na) 1996.65 

Magnesium (Mg) 14.65 

Calcium (Ca) 48.58 

Iron (Fe) 2.19 

Chlorine ' (CI) 8123.18 

Bromine (Br) 13.16 

Carbonic acid (HC0 3 ) 127.45 

Strontium (Sr) Trace 

Silica (Si0 2 ) 19.50 

5335.36 

Cc. per liter. 

Free carbonic acid in solution 92.97 

Carbonic acid in combination 40.36 

Total carbonic acid 133.33 



A considerable quantity of inflammable gas comes with the 
water. This water is considered beneficial to the health. 



*Expressed by analyst in grains per gallon, and hypothetical com- 
binations; recomputed to ionic form and parts per million at U. S. 
Geological Survey. 

Allison Lumber Company's well, about 11 miles south of Livingston, and 
3 miles south of Bellamy station, on the Southern Railway, in Section 13, 
Township 17, Range 2 W.; bored in 1903; depth, 1010 feet. Record: Soil 
and clay, 0-20 feet; black clay (Sucarnochee or Flatwoods clay), 20-160 
feet; white lime rock, 160-1000 feet; below this quicksand and water which 
overflows and yields about 3 gallons per minute. From the record it will 
be seen that the mouth of the well is on the Flatwoods clay (Tertiary), 
and that the boring, like that at Livingston, passes through the whole 



WATERS OF THE CRETACEOUS. 143 

chalk formation into the Kutaw sand. The water from this well has been 
analyzed by Mr. Hodges, and lias the following composition: 

Analysis of icater from Allison Lumber Company's well, near 

Bellamy. 



Parts per million. 

Potassium (K) 13.2 

Sodium (Na) 540.2 

Magnesium (Mg) 43.1 

Calcium (Ca) 139. (J 

Iron and alumina (Fe 2 3 , AUOi) 5.2 

Chlorine (CI) 4538.0 

Sulphuric acid (S0 4 ) .3 

Carbonic acid (HCO s ) 784.5 

Silica (Si0 2 ) 50.8 

8573.7 



Another well was bored by the same company at their logging camp, 
S miles farther south. The record was about the same as that given above, 
except that both the black clay and the lime rock were thicker, the total 
depth of the well being 1240 feet. The water rises to within 5 feet of the 
surface; on lowering the surface below that depth a small flow, less than 
half a gallon per minute, is obtained. It was thought that there was 
some leakage at the contact of the black clay with the lime rock at about 
200 feet depth, since the water rose with great force to that height. Both 
wells are cased for 40 feet, with an 8-inch hole below the casing. The 
water in the well at the logging camp is not so salty nor so highly im- 
pregnated with other minerals as that in the other well. 

Sumter Lumber Company's wells: No. 1, 4 miles southwest of Living- 
ston, in the Flatwoods; bored by F. H. Braswell; depth, 1260 feet; no de- 
tails. No. 2, 5 miles west of Livingston, also in the Flatwoods; said to be 
the only well drilled in Sumter County west of Livingston; bored by F. 
H. Braswell in 1902; never finishedl 



GREENE COUNTY. 
Surface Features. 

The Tuscaloosa formation underlies a small area, about one 
township in extent, in the northeast corner of Greene County ; 
the rest of the county is underlain by beds of the Eutaw and 
Selma chalk in belts of nearly equal width from northeast to 
southwest. Over all the older rocks wasi spread the Lafayette 
mantle of pebbles and red loam, remnants of which are still 



144 DETAILS : COASTAL PLAIN DIVISION. 

to be s'een in the high plateaus between the watercourses, where 
the country has been least affected by erosion. These high, level 
lands, 400 to 500 feet above tide, are excellent farming tracts. 
The soils are slightly less fertile than those of the prairies, but 
their level surface, their responsiveness to fertilizers, and the 
abundant s'upply of the best freestone water, stored up in the 
pebbles and sands and easily reached by wells less than 100 
feet deep or appearing as hillside springs, more than compen- 
sate for the slight difference in original fertility. In the prai- 
ries these remnants of the Lafayette mantle are not so common 
as in other sections', but here and there they form conspicuous 
features of the landscape, as for instance in the "Fork" between 
Black Warrior and Tombigbee rivers, where they appear as 
isolated conical hills upon which many oldtime mansions arc 
located. The smaller hills of this sort strongly resemble Indian 
mounds, and several of them may be seen from Burton Hill 
From the contact of the limestone with the overlying Lafayette 
sands and pebble beds, fine springs of freestone water gush out 
wherever the area of the hill is large enough to afford an ade- 
quate collecting ground. The settlement of Burton Hill is sup- 
plied in this way. 

The Lafayette is also very generally found on the third ter- 
race of the two rivers at an altitude of from 80 to 100 feet above 
the "second bottom," or lowlands. Here also, as' on the high 
plateaus, these materials are found in flat lands which are up- 
ward of 3 miles wide. The writer has been unable to discover 
any difference in structure and arrangement between the red 
loam and pebbles of this formation occurring on the high di- 
vides and those on the river terraces 200 feet below. 

From Knoxville to Eutaw the strata of the Eutaw formation 
are crossed in succession from base to top. The lower beds are 
yellow and reddish cross-bedded sands, with thin streaks and 
flakes of gray clay separating the sand layers. Above these, 
dark-gray laminated clays alternating with yellowish sands be- 
come more prominent, and near Eutaw, forming the uppermost 
strata of the formation are cross-bedded greensands. From the 
character of these materials it will be easily understood that 
the topography of the Eutaw terranes is very much broken, 
with steep rounded hills and deep gullies. The soils resulting 
from the decomposition of the Eutaw beds are usually sandy, 
but there is generally a mixture of lime with the sand by which 



WATERS OF THE CRETACEOUS. 145 

they are easily distinguishable from the Sandy soils of the La- 
fayette even when the two, as is often the case, are found in 
juxtaposition. 

At the town of Eutaw begin the beds of "rotten limestone" or 
Selma chalk, which underlie all the rest of the county westward 
to Tombigbee River. 

In the Tuscaloosa and Eutaw territory the sandy beds of 
these formations', as well as of the overlying Lafayette, are, as 
usual, a guarantee of an adequate supply of good freestone 
water, and in this part of the county, artesian wells are not very 
numerous. Of the wells in the list furnished by Judge G. B. 
Mobley, of Eutaw (see below), only thos'e around Clinton, at 
Lock 5 (now Lock 8) at Springfield, in north Eutaw, and about 
Finch's Ferry, are located in the territory of the Eutaw forma- 
tion. To these, however, may be added the wells in the city 
of Eutaw itself, which is situated at the contact of the Eutaw 
with the "rotten limestone," all these wells except those at the 
lock in the river bottom, are close to the line of contact. 

From the data given below it will be seen that only a few 
borings, in the extreme northeast corner of the county, are in 
the area of the Tuscaloosa formation. These and most of those 
just enumerated, including the deeper borings in the city of En- 
taw, penetrate into the Tuscaloosa strata. With these few ex- 
ceptions the wells of Greene County derive their waters from the 
Eutaw sands'. 

Artesiax Records. 

In the region occupied by the "rotten limestone," or Selma 
chalk the usual absence of shallow waters may be noted, and a 
correspondingly large number of artesian wells. The great ma- 
jority of these wells are located in the northeastern half of the 
belt of limestone, within io or 12 miles of the line of junction 
with the Eutaw, probably because the depth to water there av- 
erages perhaps not more than 500 to 600 feet. In the southwes- 
tern half of the limestone belt the depth to water increases to 
1000 feet and more, as shown in the Livingston well across the 
Tombigbee in Sumter County. 



in 



146 



DETAILS 



COASTAL PLAIN DIVISION. 



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152 details: coastal plain division. 

The following records may be given of wells not included in 
the above list and of some in the list of which further details 
are available. They are named in order from north to south. 

SIPSEY. 

"Well on Mose Horton's place, opposite Sipsey Mill well in Pickens 
County; depth, not recorded; water flows at 4 feet above the surface; 
yield, 15 gallons per minute; temperature, 65°. 

(LOCK 6 NOW LOCK 9) BLACK WAREIOR RIVER. 

A. P. Patton's well; bored by Kinniard in 1891; depth reported, 300 feet; 
casing, 3-inch; original flow, 20 gallons per minute; volume later fell off 
to a little over a gallon per minute; temperature, 63°. 

STEELE BLUFF. 

Well of Judge A. P. Smith, of Eutaw; bored by Morrison & Morrison 
in 1902; depth, 400 feet; casing, 3-inch; flows at 25 feet above the surface; 
volume constant; cased to 360 feet; weak flow of water from 330 feet; 
yield, 22 gallons per minute; temperature, 69°. Record: Clay, sand, 0-30 
feet; pink soapstone, 30-250 feet; sand and water, 250-400 feet. 

Well of Jeff Patton, of Knoxville, on Tombigbee River, one-half mile 
above Steeles Bluff, in the SW. 1-4, Section 12, Township 23, Range 3 E.; 
bored by Kinniard & Sample in 1901; depth, 360 feet; casing, 3-inch; first 
flowing water at 200 feet; flowed originally 50 gallons per minute, but had 
ceased before November, 1901. Record: Sand and gravel, 0-130 feet; soap- 
stone, 130-170 feet;, blue rock, 170-200 feet; sand and blue rock with water, 
200-260 feet. This well has since caved in and is lost. 

CLINTON AND VICINITY.* 

About the town of Clinton there are 28 wells, varying in depth 
from 250 to 350 feet. Most of the streams are bold and con- 
stant, the waters being very pure, with traces of salt and soda. 
Three of these wells are used to supply the boilers of the steam 
ginneries and grist mills, but the others are used solely for or- 
dinary domestic purposes. 

EUTAW AND VICINITY AND SOUTHWARD. 

The water of most of the wells about Eutaw is rather strongly 
impregnated with salt. Some of the old wells' at Finch's Ferry, 
mnetioned in Judge Mobley's list (p. 146), were used for mak- 
ing salt during the civil war. 

*See also Mobley list, page 146. 



WATERS OF THE CRETACEOUS. J 53 

The following analyses by Mr. Hodges will still better illus- 
trate the character of these waters. 

Analyses of waters from ivells near Eutaw. 



Parts per million. 

No. 1 No. 2 No. 3 No. 4 

Potassium (K) 5.2 9.8 7.6 23.4 

Sodium (Na) 221. S 193.0 430.0 1750. 

Magnesium (Mg) .5 5.3 3.0 29. o 

Calcium (Ca) 7.0 24.7 14.0 175.6 

Iron & alumina (Fe 2 O s , A1 2 3 ) 2.1 1.9 2.7 5.7 

Chlorine (CI) 232.7 220.7 515.0 2986.1 

Sulphuric acid (S0 4 ) 6 .9 1.2 3.2 

Carbonic acid (HC0 3 ) 217.6 246.7 319.7 173.7 

Silica (SiO„) 11.2 7.2 8.6 8.7 



698.7 710.2 1301.8 5156.0 



No. i.* From Crassdale plantation of J. O. Banks, Jr., 
near Eutaw, N. W. quarter N. W. quarter Section 30, Township 
22, Range 2 E. Bored in 1854. See PI. XV. A. 

No. 2.* From Little Egypt well, Crassdale Plantation of 
J. O. Banks, Jr., N. W. quarter N. W. quarter of Section 25, 
Township 22, Range 1 E. Bored by Ladd in 1899. 

No. 3. From city waterworks', Eutaw. 

No. 4.* From dump well, on Alabama Great Southern Rail- 
road, between Eutaw and Finch's Ferry. 

A record of the boring for the well at the court-house in 
Eutaw, in 1853, taken from Professor Winchell's article,* is 1 as 
follows : 

Record of Court House well, Eutaw. 

John W. Elliott, Superintendent of Work. 

Feet. 

Soil and red clay 15 

Sand and soft, light-colored, mottled clay 45 

White sand and water 3 

Blue shale and yellowish clay, alternating 200 

Yellowish clay, inclining to red 100 



*Winchell, Dr. A., Proc. Am. Assoc. Adv. Sci., Vol. 10, 1856, p. 95. 
*See also Mobley list, page 146. 



154 details: coastal plain division. 

Red, caving soil, crumbling like rotten brick-. ioo 

Sand (water), brown,* white, and greenish 20 

Red and yellowish clay 100 

Dark-brown sand 50 

Coarse reddis'h sand with gravel and scales of mica 80 

Reddish "soapstone" like a bed of clay 



743 



This record might be interpreted as follows: Soil and surface 
materials, 15 feet; Eutaw beds, 378 feet; Tuscaloosa beds, 
350 feet. In this well water, rising within a few feet of the 
surface, was found at less' than 100 feet. 

The last well sunk in the public square at Eutaw penetrated 
the red Tusicaloosa clays at the depth of 445 feet, the thick- 
ness of the clay being 40 feet. Below this, at about 480 feet, 
came a quicksand, 36 feet thick, down to the next indurated 
bed below. As soon as the quicksand was struck the water 
overflowed for an hour, but sank when the sand was agitated, 
to its present stand of -16 feet. 

Well at Alabama Great Southern Railroad depot; altitude, 
185 feet; drilled in 1886; depth, 400 feet; water s'alty; over- 
flowed at first, but has ceased to do- so. This well, starting in 
the Eutaw, penetrates the purple clays of the Tuscaloosa at 
the depth of about 400 feet. 

McClure Lumber Company's well, near the dump well No. 4 in table 

above, p. , in the W. half N. B. quarter Section 36, Township 22, Range 

2 B; now (July, 1905) boring. 

Mr. J. G. Harris's well, in the N. E. quarter Section 4, Township 21, 
Range 2 B., south of the depot in Eutaw; depth, 80 feet. 

Judge T. W. Roberts's well,* 1 mile south of Eutaw, in the N. B. quarter 
S. E. quarter Section 4, Township 21, Range 2B; diameter at bottom, 
1 1-2 inches; depth, 239 feet; first water reported at 52 1-2 feet; water supply 
at bottom; flows at surface; carries some salt; starts in Selma chalk and 
probably gets water in the Eutaw sands. Record: Clay and sand to 
lime rock, 11 feet; rotten lime rock (water at bottom), 39 feet; bMe 
lime rock, 150 feet; sand, 10 feet; dark soapstone, 16 feet; sand, 3 feet; 
soapstone, 6 feet; hard rock, 2 feet; sand to water, 2 feet. 

Well on Clarke place (owned by Ed. and Henry Kinney) in the N. W. 
quarter N. E. quarter Section 9, Township 21, Range 2, 1 1-2 miles south 
of Eutaw, 500 yards from well of Judge T. W. Roberts; bored by Gus. 
Sample in May, 1905; depth, 520 feet; 3-inch casing; flows small stream; 
pump used; blue marl encountered at 16 feet, continuing for 500 feet. 

*See also Mobley list, page 146. 



WATERS OF THE CRETACEOUS. 155 

Well on Crenshaw place, formerly F. I-. Constantine's, in the S. 10. quar- 
ter S. E. quarter Section 9, Township 21, Range 2 B., about 2 miles south 
of Eutaw; bored for Eugene Anderson In May, L905, by Gus. Sample; 
depth. Mil feet; 2 1-2-im-h casing'; lirst water, at 35 feet, rose to surface; 
overflowing water at tiO feet and bold (2 1-2-inch) stream at 105 feet. 

Well on J. \Y. Hall place, owned by Marion James (colored), in Section 
15. Township 21. Range 2 E.. about 3 miles south of Eutaw; bored in 
1904; depth, 300 feet; 3-inch casing; flows a fine stream. 

Wells on Clements place,* about 4 1-2 miles south of Eutaw, in the N. 
W. quarter Section 21. Township 21. Range 2 E. (old wells): No. 1, on 
Eutaw and Forkland road; yield, 2 gallons per minute; temperature, 71°, 
water salty. No. 2, one-half mile east of road; deptn. 200 feet; twenty- 
five years ago gave a strong stream, but has gradually weakened; pres- 
ent overflow 9 feet lower than formerly; yield, 1 2-3 gallons per minute; 
temperature. 71°; water salty. No. 3. 100 yards from house; flow exceed- 
ingly small. 

Wells on Judge T. W. Coleman's place (formerly Jos. W. Hall's): 
No. 1. in the S. W. quarter N. W. quarter Section 33, Township 21, Range 
2 E.. 6 miles south of Eutaw; bored in the fall of 1904 by Gus. Sample; 
depth, 485 feet; flows 1 1-2-inch stream. No. 2, in the W. 1-2 N. E. quarter 
same section; completed in June, 1905. 

Judge T. W. Robert's well, in the S. E. quarter section 33. Township 21, 
Range 2 E., about 6 miles south of Eutaw; bored in the spring of 1905 
by Gus. Sample; depth, about 450 feet; flows a strong stream. An old 
well with a very weak flow, on the same place is mentioned above in the 
Mobley list (p. 146.) 

Well of Dollarhide Company, in the W. half N. W. quarter Section 2, 
Township 20, Range 2. E., on top of hill half a mile west of the old well 
in section 1 (see Mobley list), which is in the swamp; bored in November 
1904. by Gus. Sample; depth, about 500 feet. This well is about 75 feet 
higher than the old well, but flows a stronger stream. 

Judge T. W. Roberts's well.j 7 miles south of Eutaw, in Section 3, 
Township 20, Range 2 E.; bored by Kinniard & Sample in 1901; depth, 405 
feet; casing, 4 1-2-inch; water at 300 feet, salty; yield, 10 gallons per minute 
at surface; temperature, 70°. An old well near by this. 

Wells on Swilley place, 9 miles south of Eutaw, owned by E. W. De- 
grauenreid, of Greensboro: No. 1, at the house, in the S. E. quarter N. W. 
quarter Section 7, Township 20, Range 2 E.; bored by Morrison in 1898; 
depth, 495 feet; casing, 3-inch; yield, 2 gallons per minute; temperature, 
71°; flow obtained from 400 feet; water very salty; used for domestic 
purposes and stock. Record: Clay. 0-10 feet; blue rock, 10-250 feet; sand, 
with thin strata of blue rock and water, 250-495 feet. No. 2. 1 mile north- 
east of the house, in the S. E. quarter N. W. quarter Section 7, Township 
20. Range 2 E. ; reported by Morrison in 1898; depth, 450 feet; casing, 3-inch; 
yield, 1 gallon per minute; temperature, 71°; flow from 400 feet; water 
salty. Record: Clay, 0-10 feet; blue rock, 10-300 feet; hard rock, 300-306 
feet; sand, with water, 306-450feet. 

S. L. Creswell's wells, 10 miles southwest of Eutaw, in Section 17, 
Township 20, Range 2 E. : No. 1. depth, 456 feet; temperature, 72°. No. 

2. in field at Creswell's plantation; depth, 440 feet; temperature, 71°. No. 

3, one-half mile north of No. 1,; depth, 550 feet; temperature, 72°. 



*See also Mobley list, page 146. 
tSee also Mobley list, page 146. 



156 DETAILS : COASTAL PLAIN DIVISION. 

C. C. Dunlap's well, in center of Section 17, Township 20, Range 2 E.; 
recently bored; depth, over 400 feet; good flow. 

Capt. James Webb's well, 11 miles south of Eutaw, in Section 20, 
Township 20, Range 2 E. ; bored by Kinniard & Sample; depth, 560 feet; 
casing, 4-inch; first flowing water at 540 feet; well flowed a year and then 
partly caved in, after which the pump had to be used. Record: Soil, 
0-6 feet; blue rock, 6-540 feet: sand, 540-560 feet. 

Old wells renewed— On the Thornton place, in the N. E. quarter Sec- 
tion 25, Township 20, Range 1 E., an old well has been rediscovered which 
now yields a plentiful supply of salty but palatable water. 

On the E. C. Seldon place, in Section 12, Township 21, Range 1 E., an 
old well was exposed by the formation of a gully. The well was found 
plugged up, but when opened the water stood 6 or 8 feet below the sur- 
face. It is near the house and is now used for domestic purposes. It is 
supposed to have been bored about 1840. No one in the vicinity remem- 
bered anything about it. 

In the northern edge of Eutaw, about ten years ago, a freshet exposed 
an old well that was bored about 1845 by Colonel Pickens. This well now 
gives a good supply of fine drinking water. 

In the vicinity of Eutaw are several old bored wells that have been 
converted into serviceable open wells by cutting off the old wooden casing 
after it has begun to decay, and digging around it to a sufficient depth. 

The well on the Jones place, in the N. E. quarter Section 8, Township 
21, Range 2 E., has the reputation of yielding a fine sulphur water. 

HAIRSTON. 

About 2 1-2 miles east of Hairston is a well, owner unknown, that is re- 
ported to be 530 feet deep. Blue rock, 170 feet thick; water rises to 2 1-2 
feet above the ground; yield, 4 gallons per minute. 

BOLIGEE AND VICINITY. 

Well of Moses Kay (colored), 4 miles north of Boligee; bored by Mr. 
Ladd in 1899; depth, 142 feet; casing, 3-inch; pure water, 2 gallons per min- 
ute, from bottom; flows 3 feet above the surface; temperature, 66°; lime- 
stone occurs at 40 feet. 

Well of Alec. Alexander (colored); bored by Mr. Ladd in 1899; depth, 350 
feet; water, which rises to 5 feet above the surface, was obtained at 
320 feet. 

E. P. Bouchelle's well, Boligee; bored in 1899 by Mr. Ladd; depth, 500 
feet; first flowing water at 300 feet; water rises to 22 feet above the 
ground; flow originally 60 gallons, but June 20, 1899, was 40 gallons per 
minute; somewhat salty; temperature, 70°; closed against sand at the 
bottom; starts in Selma chalk; water supply from Eutaw sand. 

H. T. Bouchelle's well, in the S. E. quarter Section 31, Township 21, 
Range IE.; bored by J. I. Hawk, in 1898; depth, 450 feet; 3-inch casing; 
closed against sand; flowed over pipe at 10 feet above the ground; esti- 
mated original volume, 10 gallons per minute; first flowing water at 350 
feet; somewhat salty. Record: Soil, 0-20 feet; blue rock, 20-220 feet; sand, 
with occasional thin layers of rock, with water, 220-450 feet. 

Dr. Hatter's well, depth, 250 feet; flow small; starts in Selma chalk 
and obtains its water from Eutaw sands. 

Mrs. Perry's well, 100 yards south of station; bored by Mr. Ladd in 
1894; flows 3 feet above surface; yield, 1 3-4 gallons per minute from a depth 
of 250 feet; water carries salt and sulphur; temperature, 68°. 



WATERS OF THE CRETACEOUS. 157 

BURTON KILL. 

Dr. Perrin's well, in the S. W. quarter Section 13, Township 20, Range 
1 E. ; not flowing:; depth, 544 feet; temperature, 70°. 

Bullock well, in the N. E. quarter Section 14, Township 20, Range 1 E. ; 
flows small stream. 

ERIE AND \ ICINITY. 

Well of Caleb Blackmail (colored). 2 1- miles southwest of Erie, bored 
by Morrison in 18S8; depth, 320 feet; casing, 4-inch; water from 290 feet, 
flowing 10 gallons per minute to a height of 5 feet above the ground; 
temperature, 67°. Record: Sand and gravel, 0-30 feet; blue rock, 30-300 
feet; sand, water, blue rock, etc., 300-330 feet. 

Well of Deb Marks (colored), 3 miles southwest of Erie, in Section 30, 
Township 20. Range 3 E. ; bored by Morrison in 1898; depth, 330 feet; 
casing, 3-inch; water from 300 feet, flowing 4 1-2 gallons per minute; 
temperature. G8°. Record: Sand and gravel, 0-30 feet; blue rock, 30-300 
feet; sand with water, 300-330 feet. 

FORKLAND AND VICINITY. 

Miss C. A. Lewis's well, in the N. W. quarter N. W. quarter Section 3, 
Township 19. Range 2 E.; bored in 1901 by J. I. Hawk; water soft, not 
salty; originally the well gave a strong flow, but an accident in inserting 
the casing greatly reduced it; present flow, 1 1-2 gallons per minute; 
temperature, 72°. 

E. S. Latimer's well, in the S. E. quarter S. W. quarter Section 4, 
Township 19, Range 2 E.; bored by J. I. Hawk in 1901; flows 9 gallons per 
minute; temperature. 74°; water salty but soft and gives no crust in 
boilers; volume constant; water rises to 18 feet above the ground; cased 
throughout, except in the limestone; water used for domestic purposes. 

Williamson Glover's well, Forkland; depth, 445 feet; temperature, 72°. 

D. S. Brassfield's well, at Landing, in the N. W. quarter Section 14, 
Township 19, Range 2 E. ; depth, 575 feet; blue rock 350 feet thick; water 
rises to 3 feet above the ground; yield, 20 gallons per minute. 

W. B. Baltzell's well. 5 miles west of Forkland, in the W. half N. W. 
quarter Section 11, Township 19. Range 1 E.; bored by Hawk in 1891; 
flow, 8 gallons per minute; .emperature. 72°. 

Emma R. Hillman's well, on the Robert Taylor place, in the W.half 
N. W. quarter Section 17, Township 19, Range 1 E. ; flows a bold stream; 
water slightly salty but paiatable. 

Wells on Cole place.* in Seccion 25, Township 19, Range 2 E.; 4 1-2 
miles north of Demopolis, on the Erie road (old wells): No. 1, flow, 1 
gallon per minute; temperature. 70°. Three others within a radius of 1 
mile; all flow about the same stream. 



158 DETAILS : COASTAL PLAIN DIVISION. 

HALE COUNTY. 
Surface Features. 

The surface of Hale County is divided somewhat evenly 
between strata of the Tuscaloosa formation in the northeast, 
the Eutaw in the center, and the Selma chalk in the southwest. 
Over all these rocks were spread the pebbles' and red loam of 
the Lafayette ; but this mantle has been in great part removed 
by erosion from the area of the chalk, though present over most 
of the other two divisions. Where the county is least dissected 
by erosion, especially on the wide divides between the streams, 
the surface is' quite level, with a soil of red loam underlain by 
pebbles, the two together being from 20 to 25 feet thick. Along 
the slopes from this plateau, the underlying formations are ex- 
posed. Wherever the Lafayette pebbles and loam are present, 
and very generally in the two prevailingly sandy formations, 
Tuscaloosa and Eutaw, there is seldom any lack of good water 
to be had from ordinary wells and from springs. 

Among the many fine springs of this 1 county a few may be 
mentioned. The best known of all are the Green Springs, in 
the S. W. quarter Section 23, Township 22, Range 4 E., near 
the celebrated school of Prof. Henry Tutwiler, about one-quar- 
ter of a mile from Fivemile creek. Here are several bold 
springs of the finest chalybeate water. Farther down the creek, 
4 or 5 miles from Green Springs, are the Linkumdoddy Springs 
(chalybeate and sulphur), also well known. 

ArtesialV Wells. 

In the region, occupied by the Selma chalk, the surface wa- 
ters as usual, are not sufficient for the needs', of the people, and 
recourse is had to artesian wells. A few of these wells are lo- 
cated in the Tuscaloosa area and get their water supply from 
its sands ; and others' located near the eastern edge of the Eutaw 
outcrop also penetrate the water-bearing sands of the Tusca- 
loosa. Of this character are the wells at Moundville, Powers, 
Cypress Switch, and Stewarts, on the Alabama Great South- 
ern Railroad. Others located on the Eutaw outcrop, especially 
those nearest to the chalk territory, are sunk altogether into 
Eutaw materials and there obtain their water supply. 



WATERS OF THE CRETACEOUS. 159 

Most of the wells along the line of the Southern Railway 
between Akron and Selma are thus situated, e. g., Akron, Evans, 
Greenwood, (Wedgworth), Sawyerville, and Greensboro. 
But the great majority of the wells, especially in the western 
and southern parts of the county, are located on the Selma 
chalk outcrop, though the borings pass through that formation 
and get their water supply from the underlying Eutaw sands'. 

The following records of the artesian wells' in Hale County 
are given as nearly as possible in their geographic order, from 
north to south. 

MOUNDVILLE AND VICINITY. 

Thos. B. Allen's well, near the lower line of Tuscaloosa County, S 
miles west of Moundville, on the left bank of Black Warrior River; 
bored about 1903; depth, 275 feet; first 50 feet, down to a soft rock, cased 
with 3-inch pipe, the rest to bottom with 1 1-4-inch pipe; first overflow at 
234 feet; water rises above the surface, making a noise like an engine 
pumping; yield, 24 gallons per minute; temperature. G3°. The water is 
piped over house, kitchen, dairy, and garden. An analysis by Mr. Hodges 
is as follows: 

Analysis of water from Thos. B. Allen's well, near Moundville. 



Parts per million. 

Potassium (K) 11.8 

Sodium (Na) 295.6 

Magnesium (Mg) 20.7 

Calcium (Ca) 109.8 

Iron and alumina (Pe,0 3 , AU0 3 ) 1.7 

Chlorine (CD 649.6 

Sulphuric acid (S0 4 ) .6 

Carbonic acid (HC0 3 ) 115. 6 

Silica (Si0 2 ) 15.9 

1221.3 



J. A. Elliott & Son's well, bored by Morrison in 1899; depth, 600 feet; 
water at 450 feet, rose to -1 foot and pumping was necessary for five min- 
utes; on stopping the pumping the well began to flow and has since con- 
tinued; yield, 1 gallon per minute; temperature, 67°. Well is in Tuscaloosa 
formation. Record: Soil and clay, 0-50 feet; sand rock, 50-54 feet; pink' 
soapstone, 54-300 feet; hard rock, 300-310 feet; sand, with water and 
occasional strata of hard rock, 310-600 feet. The composition of this water 
as shown by the analysis of Mr. Hodges, is as follows: 



160 details: coastal plain division. 

Analysis of water from J. A. Elliott & Son's well, Moundville. 



Parts pei* million. 

Potassium (K) 3.3 

Sodium (Na) 2.9 

Magnesium (Mg) 5.5 

Calcium (Ca) 23.8 

Iron and alumina (Fe 2 3 , A1 2 3 ) 2.0 

Chlorine (Gl) 4.2 

Sulphuric acid (S0 4 ) 4.3 

Carbonic acid (HC0 8 ) 100.0 

Silica (Si0 2 ) 19.2 

165.9 



R. L. Griffin's well, bored by W. H. Martin in 1903; depth, 480 feet; 
casing, 70 feet of 3-inch, 360' feet of 1 1-4-inch; water at 375 feet, rose to 
-1 foot; at 480 feet, rose to 16 feet above the ground; present yield lOi 
gallons per minute; temperature, 67°; water used in several houses. 
Record: Clay, 0-70 feet; blue rock, 70-375 feet. 

W. P. Phifer's well, in the S. W. quarter Section 1, Township 23, Range 
4; bored in ^ugust, 1903, by W. H. Martin; depth, 490 feet; cased 63 feet 
with 3-inch casing, 400 feet with 1 1-4-inch inner casing; flow, 12 gallons 
per minute. , 

POWERS STATION AND VICINITY. 

John Findlay's well, Powers; bored by W. V. Morrison; depth, 406 
feet; casing, 3-inch; flow at 330 feet; yield, 7 1-2 gallons per minute, 
volume constant; water rises to 25 feet above tne ground; temperature, 
68°. Record: Soil and clay, 0-500 feet; blue rock, 50-250 feet; sand and 
water, Wj.- thin strata of rock, 250-406 feet. 

Wells at Lock 6 (now Lock 9), on Black Warrior River near Powers, 
in fraction D, Section 5, Township 23, Range 4; bored by Morrison in 
1900, for Christie, Lowe & Hey worth, contractors: No. 1, depth, 316 
feet; 3-inch casing; original volume, 30 gallons; water rose to 34 feet 
above the ground; weak overflow at 296 feet; temperature, 65°. Record: 
Sand and gravel, 0-50 feet; soapstone, 50-200 feet; water, sand, occasional 
thin strata of rock, 200-316 feet. No. a, is a 1 1-2-inch pipe inside of 
well No. 1; depth, 336 feet; volume said to be variable; flow, 6 gallons per 
minute; temperature, 65°. 

CYPRESS SWITCH. 

Strudwick Brothers' well, bored by W. J. Kinnaird in 1900; depth, 320 
feet; diameter, 2 inches; water at 300 feet, rising to 20 feet above the 
ground; temperature, 67°. 

STEWARTS AJ\D VICINITY. 

C. D. Cummings's wells: No. 1, at house; bored by Morrison in 1897; 
depth, 605 feet; diameter, 3 inches; water at 600 feet, rising to 35 feet 
above the ground; flow, (30 feet above the ground), 6 gallons per minute; 
volume constant; temperature, 66°; water hard (salt and sulphur), Record: 



WATERS OF TI1K CRETACEOUS. 161 

Soil and clay. 0-30 feet; pink soapstone, 30-600 feet. No. 2, 250 yards north 
of house; bored by Morrison in 1900: depth, 400 feet; diameter. 3 inches; 
water at 350 feet, rising to 30 feet above the ground; decidedly mineral 
(chalybeate), with odor of hydrogen sulphide; record same as in No. 1. 
No. 3. 300 yards north of house; bored by Morrison in 1897; depth, 363 
feet; diameter, 3 inches; water at 300 feet, rising to 30 feet above the 
ground; flow. 2 gallons per minute; volume, constant; temperature, 67°; 
water hard and decidedly mineral (chalybeate); record same as in No. 1. 

W. 11. Martin's well, about 2 1-2 miles east of Stewarts; bored by Martin 
& Morrison; depth, 550 feet; diameter, 3 inches; water stands at -39 
feet; level constant. Record: Soil and clay, 0-30 feet; sand and gravel, 
30-400 feet; rock. 400-402 feet; black mud, 402-412 feet; rock, 412-413 feet; 
successive strata of rock and black or red mud, 413-550 feet. 

Wells at Lock 5 (now Lock S). between Stewarts and Akron; No. 1, 
drilled in 1899; diameter, 3 inches; depth, 160 feet; flow, 60 gallons per min- 
ute; quality good; well entirely in Tuscaloosa beds. No. 2, (owner un- 
known), reported to be 600 feet deep, the water standing at 8 feet above 
the ground. 

All the wells above given are located on and derive their water from 
the Tuscaloosa strata. 

AKRON AND VICINITY. 

W. B. Inge's well, at tne hotel, Akron; depth, 140 feet; water level varies 
from -6 feet in dry weather to above the ground in wet weather; for- 
merly overflowed a foot or more above the surface; yield, 7 gallons per 
minute; temperature, 68°. This well is located on the Eutaw sands, 
but gets waater from the underlying Tuscaloosa beds. 

Well of the Alabama Great Southern Railroad, northeast of depot at 
Akron. This well was bored about the year 1904 or 1905; no record avail- 
able. 

Wells of Waller. Lichtman, and Murphy Land and Development Com- 
pany. 

In 1905 seven wells were bored by this company on their property at 
Akron. Depths varying from 146 to 305 feet or more. Records have been 
obtained of only one of these wells in which three water-bearing sands 
were penetrated at depths of 146 feet, 200 feet, and 305 feet. It being 
thought that there was marked difference in the quality of these three 
flows, each was cased off, so that it is separately delivered at the mouth 
of the well, and designated No. 1, No. 2, and No. 3 respectively. Casing, 
3-inch down to No. 1, 146 feet; inside of this 2-inch casing down to flow 
No. 2, 200 feet; and inside the 2-inch casing 305 feet of 1 1-4-inch casing 
to the lowest water, 305 feet. Record; Soil, clay and gravel. 0-83 feet; 
blue soapstone, 83-116 feet, waterbearing sands ,116-146 feet, (yielding water 
No. 1); strata not recorded, 146-190 feet; blue soapstone 190-200 feet; below 
this soapstone good flow, (No. 2): strata not recorded, 200-250 feet; 
pink soapstone or kaolin, 250-305, below which (No. 3,) a fine stream flow- 
ing about 12 feet above the ground through the well tools. 

The waters from No. 1 and No. 2 have been analyzed by Mr. Hodges 
with results given below. No. 1 and No. 2 come from Eutaw sands; 
No. 3 from the Tuscaloosa sands. 



11 



162 DETAILS : COASTAL PLAIN DIVISION. 

Analysis of waters from Waller, Lichtman, and Murphy Land Co. 
well, Akron. 



Parts per million. 

Potassium (K) 4.3 3.0 

Sodium (Na) 8.1 6.6 

Lithium (Li) Trace Trace 

Magnesium (Mg) .3 .3 

Calcium (Ca) 7.0 8.2 

Iron (Fe) 13.6 10.0 

Alumina (A1 2 3 ) 1.8 1.6 

Chlorine (CI) 3.1 4.1 

Sulphuric acid (S0 2 ) 5.2 5.8 

Carbonic acid (HCO s ) 68.6 56.2 

Silica (SiO a ) 17.7 19.6 

141.4 115.1 



Prom the analysis it will be seen that this is one of the strongest chaly- 
beate waters as yet tested in the state. 

Well at house of W. E. Wedgworth, 1 mile south of Akron, in the N. 
W. quarter N. E. quarter Section 19, Township 22, Range 4 B.; bored by 
Sample in 1902; depth, 400 feet; diameter, 3 inches; water stands at -15 
feet; level constant under uomestic use;' temperature, 66°. 

O. V. Crabtree & Co's. well, 3 miles west of Akron, on Alabama Great 
Southern Railroad; bored by Kinnaird & Sample in 1900; depth, 300 feet; 
casing 3-inch; flowing water at 220 feet, rising to 8 feet above the ground. 
Record: Soil and gravel, 0-50 feet; blue rock, 50-220 feet; sand with water, 
220-300 feet. 

Judge Coleman's wells, near Akron, and between Akron and Finch's 
Ferry: No. 1, 1 mile north of the Crabtree well above described; bored 
.. y Martin in 1904; depth, 324 feet; estimated yield, 25-30 gallons per minute; 
contains iron and salt; temperature, 67°. No. 2, 75 yards from No. 1; 
record same in all particulars. No. 3, on the Bartee place, ± 1-4 miles west 
of the two preceding; bored in 1903; depth, 354 feet; casing, 39 feet, 3-inch; 
estimated flow, 50 gallons per minute. No. 4, 2 miles east of Finch's 
Ferry; bored in 1903; depth, 278 feet; casing, 39 feet, 3-inch; estimated 
flow, 12 gallons per minute. No. u, 1 1-2 miles southeast of Akron; bored 
in 1904; depth, 600 feet; water level, -13 feet. This well is half a milq 
east of the Southern Railway track, and the surface at the mouth of 
the well is estimated to be 15 feet higher than tne track. 

EVANS STATION AND VICINITY. 

B. S. Evans's wells, Evans station: No. 1, 200 yards from house, in 
the N. E. quarter Section 36, Township 22, Range 3 E. ; bored by W. J. 
Kinnaird in 1901; depth, 200 feet; flowing water at 180 feet, rising to 8 
feet above the ground; yield, 30 gallons per minute, constant; temperature, 
68°. No. 2, at house; bored by Morrison; depth, 633 feet; 4-inch casing 
above 40 feet; water level -3 feet; used for domestic purposes. Record: 
Sand and clay, 0-40 feet; blue rock, 40-300 feet; sand, 300-350 feet; soap- 
stone, 350-633 feet. 

W. M. Wedgworth's wells, on McGee place, three-fourths of a mile 
east of Evans station; bored in 1904 by Martin & Wyndham: No. 1, depth, 
400 feet water level, -1 foot. No. 2, 100 yards north of No. 1; depth, 300 
feet; water level. -12 fe^t. 



WATERS OF THE CRETACEOUS. 163 

W. M. Sample's wells: No. 1, at Evans station; bored by Kinnaird & 
Sample in 1902; depth, ISO feet, casing, 3-inch; flowing water at 100 feet; 
rising to 4 feet above the ground; yield, 18 gallons- per minute; slightly 
diminished since first bored; temperature, 68°. Record: Soil and clay, 
0-40 feet; blue rock, 40-160 feet; sand with water, 160-180 feet. No. 2, one- 
fourth of a mile west of Evans station; bored Dy Kinniard & Sample; 
depth, 180 feet; casing, 3-inch; flowing water at 160 feet; original volume, 
10 gallons per minute, decreased slightly; temperature, 68°. Record: 
Soil and clay, 0-70 feet; blue rock, 70-160 feet; sand with water, 160-180 
feet. No. 3, one-half mile west of Evans station; bored by Kinniard & 
sample; depth, 160 feet; casing, 3-inch; flowing water at 140 feet; orig- 
inal volume, 30 gallons per minute; present volume, 18 gallons per minute; 
temperature, 67°. Record: Soil and clay, 0-70 feet; blue rock, 70-140 
feet; sand with water. 140-160 feet. No. 4, three-fourths of a mile west 
of Evans station; bored by Kinniard & Sample; depth, 200 feet; casing, 
o-inch; flowing water at 160 feet; volume, 30 gallons per minute (esti- 
mated); temperature, 6S°. Record: Soil and clay, 0-50 feet; blue rock, 
50-120 feet; (?), 120-160 feet; sand, with water, 160-200 feet. 

C. D. Cummings's well, three-fourths of a mile west of Evans station; 
bored by Sample & Morrison in 1902 (?); depth, 160 feet; casing, 3-inch; 
water rises to 4 feet above the ground; yield, 3 1-2 gallons per minute; 
temperature. 68°. Record: Sand and gravel, 0-60 feet; blue rock, 60-155 
feet; coal, 155-156 1-2 feet; sand, with water, 156 1-2-160 feet. 

C. H. Wedgworth's well, about 1 1-4 miles west of Evans station, in 
the S. W. quarter S. E. quarter Section 34, Township 22, Range 3 E. ; 
bored by Kinnaird & Sample in 1901; depth, 210 feet; casing, 3-inch; 
water at 160 feet, rising to 4 feet above the bround; volume, 24 gallons 
per minute; temperature, 67°. Record: Sand and gravel, 0-40 feet; 
blue rock, 40-160 feet; sand, with water, 160-210 feet. 

WEDGWORTH, (GREENWOOD, MAYS STATION.) 

These are all the same locality. The railroad station is 
Mays ; the postoffice was Greenwood until very recently, when 
the name was changed to Wedgworth. 

W. M. Wedgworth's well, in the S. W. quarter N. W. quarter Section 
11, Township 21, Range 3 E.; bored Oy Sample & Morrison in 1899 or 
1900; depth, 200 feet; casing, 4 1-2-inch; flowing water at 140 feet, rising 
to 10 feet above the ground; volume constant; decided improvement in 
the health of users; yield, 18 gallons per minute; temperature, 68°. 
Record: Sand and gravel, 0-30 feet; blue rock, 30-140 feet; sand and water, 
140-150 feet; blue rock, 150-190 feet; sand and water, 190-200 feet. The 
analysis of this water, by Mr. Hodges, shows the following composition: 



164 details: coastal plain division. 

Analysis of water from W. M. WedgworWs well, near Wedgworth. 



Parts per million. 

Potassium (K) 7.6 

Sodium (Na) 24.6 

Magnesium (Mg) 2.2 

Calcium (Ca) 11.9 

Iron and alumina (Fe 2 3 , AL0 3 ) 2.6 

Chlorine (CI) 10.5 

Sulphuric acid (SO*) 5.1 

Carbonic acid (HCO s ) 88.4 

Silica (Si0 2 ) 17.2 

170.1 



Well at Wedgworth's store, on the railroad; bored in 1904 by Kinnaird 
& Sample; depth, 235 feet; 40 feet of 3-inch casing; first flowing water 
at 175 feet; second flow, good stream, at 200 feet; third water at 235 
feet, rising to 15 feet above the ground. 

Miss K. C. May's well, 3 miles north of east of Wedgworth; b6red by 
Kinnaird & Sample in 1902; depth, 200 feet; diameter, 3 inches; flowing 
water at 160 feet; estimated volume, 65 gallons per minute; flow constant; 
temperature, 67°. Record: Soil, etc., 0-40 feet; blue rock, 40-160 feet; 
sand, with water, 160-200 feet. 

W. B. Wedgworth's wells: No. 1, 1 mile east of Wedgworth, in the N. 
E. quarter N. W. quarter Section 1, Township 21, Range 3 E. ; bored by 
Sample in 1902; depth. 2i0 feet; casing, 3-inch; flowing water at 170 feet, 
rising to 5 feet above the ground; yield. 18 gallons per minute; tempera- 
ture, 67°. Record: Soil and clay, 0-40 feet; blue rock, 40-170 feet; sand, 
with water, 170-210 feet. No. 2, about 1 1-4 miles east of Wedgworth, on 
the old Wedgworth place; water rises to 4 feet above the ground; 
yield, 35 gallons per minute; temperature, 67°; other data similar to No. 1. 

Wells on Allen Wilson place: No. 1, one-half mile west of Wedgworth; 
flow, 2 1-2 gallons per minute; temperature, 68°. No. 2, 1 1-2 miles west 
of Station; flow, 4 1-2 gallons per minute; temperature, 67°. 

Governor Seay's well, 3 miles southwest of Wedgworth, on the road 
to Lock 4 (7); drilled about 1897; depth, 198 feet; casing, 30 feet, 6-inch; 
water rises to 3 feet above the ground; yield, 15 gallons per minute; 
temperature, 66°. 

E. W. Degraffenreid's well, 4 or 5 miles southwest of Wedgworth; 
yield, 2 1-4 gallons per minute; temperature, 68°; an old well, but still 
flowing. 

E. L. Kimbrough's wells, 3 to 5 miles southwest of \vedgworth; No. 1 
("camp well"), one-fourth of a mile east of Lock 4 (7), in pasture; bored 
by Morrison; depth, 160 feet; diameter, 3 inches; flowing water at 140 
feet, rising to 4 feet above the ground; yield, 40 gallons per minute; 
flow, constant; temperature, 67°. Record: Soil and clay, 0-53 feet; blue 
rock, 53-130 feet; sand and water, 130-140 feet; hard white rock, 140-160 
feet. No. 2 ("new-ground well"), in swamp 1 1-4 miles east of Lock 4 
(7>; originally bored by hand and afterwards (1898) deepened by Morri- 
son to 160 feet; casing, 30 feet, 6-inch; estimated original flow at 3 feet 
above the ground; 35 gallons per minute; present flow, 12 gallons per min- 
ute; temperature, 67°. No. 3, ("upland-pasture well"), bored by Morri- 
son in 1898; depth, 160 feet; casing, 4 1-2-inch; flowing water at 140 feet; 
estimated original yield, 20 gallons per minute; present yield, 17 gallons 
per minute; temperature, 68°. No. 4 ("river-field well"), bored by J. I. 



WATERS (>F THE CRETACEOUS. 165 

Hawk in 1S96; depth, isr. feet; llowing water at 175 feet; yield, 12 gallons 
per minute; temperature, 08°. Record: Clay ana soil, 0-10 feet; quick- 
sand, 10-40 feet; blue rock, 40-185 feet. No. 6 (."house-lot well"), bored 
by J. 1. Hawk in 1898; depth, 272 feet; first water at 175 feet; ftowtirvg 
water at 240 feet; estimated original yield, 18 gallons per minute; present 
yield, 3 gallons per minute; temperature, G8°. Record: Sand, clay, and 
gravel, 0-25 feet; blue rock, 25-175 feet; remainder unrecorded. No. 6 
("mill well"), bored by J. I. Hawk; yield, 17 gallons per minute; tempe- 
rature, 68°. 

Wells of Madison Jones, Jr.. No. 1. at Mays station (Wedgworth. 
Postoffice); bored by J. I. Hawk in 1899; depth. 216 feet; casing, 6-inch; 
flow, CO gallons per minute; volume constant; temperature, 69°; well is 
entirely within the Eutaw sands. Record: Clay, 0-12 feet; blue rock, 
12-170 feet; sand and water, with thin strata of blue rock, 170-216 feet. 
No. 2, in pasture opposite the house, half a mile south of the station; 
bored 170 feet by hand, and completed by J. I. Hawk in 1899; depth, 285 
feet (256 feet according to Mr. Jones); casing. 5-inch; flows 22 gallons 
per minute; volume constant; temperature, 69°. The water from this 
well shows the following composition in the analysis by Mr. Hodges: 

Analysis of water from well of Madison Jones, Jr., near Mays Station. 



Parts per million. 

Potassium (K) 3.9 

Sodium (Na) 51.8 

Magnesium (Mg) 2.6 

Calcium (Ca) 12.3 

Iron and alumina (Fe>0 3 , AU0 3 ) 2.5 

Chlorine (CI) 38.4 

Sulphuric acid (S0 4 ) 5.0 

Carbonic acid (HC0 3 ) 121.2 

Silica (Si0 2 ) 27. S 

265.5 



LOCK 4 (NOW 7.) 

Well No. 1, in the S. W. quarter of Section 18, Township 21, Range 3 E.; 
bored by Morrison in 1900; depth, 2S0 feet; casing, 40 feet, 3-inch; first 
flowing water at 200 feet; estimated original yield, 35 gallons per min- 
ute; present yield, 18 gallons per minute; temperature, 6t>°; water rises 
to 24 feet above the ground. Record: Sand and gravel, 0-50 feet; blue 
rock, 50-160 feet; sand with water alternating with thin strata (10-12 feet( 
of blue rock, 160-180 feet. Well No. 2, on west bank of river; bored by 
N. A. Yuille; covered by water in times of flood; data not obtainable. 

The analysis of the water from well No. 1, by Mr. Hodges, is as fol- 
lows: 



166 details: coastal plain division. 

Analysis of water from well No. 1, at Lock 4 (now Lock 7.) 



Parts per million. 

Potassium (K) 4.5 

Sodium (Na) 444.8 

Magnesium (Mg) 2.7 

Calcium (Ca) 14.9 

Iron and alumina (Fe 2 3 , AL.O?) 1.6 

Chlorine (CI) 481.9 

Sulphuric acid (S0 4 ) .4 

Carbonic acid (HCO s ) 413.6 

Silica (Si0 2 ) 13.2 

1377.6 



SAWYERVILLE AND VICINITY. 

"B. L. Kimbrough has two deep wells at Sawyerville, bored by J. I. 
Hawk. 

Jack Monette's wells, 3 miles west of Sawyerville: No. 1, at mill; 
bored by Sample & Morrison in 1897; depth, 640 feet; diam,eter, 3 inches; 
water stands at -8 feet; level constant. Record: Sand, 0-10 feet; blue 
rock, 10-450 feet; sand and water, with thin strata of blue rock, 450-600 
feet; pink soapstone, 600-640 feet. No. 2, at house; bored by Sample in 
1901; depth, 440 feet; flowing water from bottom; yield, 17 gallons per min- 
ute; volume constant; temperature, 70°. No. 3, at mill; bored by Sample; 
depth, 440 feet;' diameter, 3 inches; water stands at constant height of 
-10 feet. No. 4, at mill; bored by Smith; depth, 435 feet; diameter, 3 
inches; water stands at constant height of -10 feet. No. 5, one-fourth 
of a mile east of Lock 3 (now Lock 6); bored by Smith; depth, 360 feet; 
casing, 1 1-2-inch; flows about 4 gallons per minute; temperature, 69°. 
No. 6, one-half mile northeast of Lock 3 (now Lock 6); drilled by Smith; 
data lacking. Mr. Monette has also three overflowing wells at old Erie, 
of which records were not obtained. 

T. J. Yancey's well, 3 miles nearly south of Sawyerville, in Section 13, 
Township 20, Range 3 E.; bored by Kinnaird & Sample in 1902; depth, 
315 feet; casing, 30 feet, 3-inch; first overflow at 280 feet, weak; water 
rises to 5 feet above the ground; yield 15 gallons per minute; tempera- 
ture, 67°. Record: Sand and gravel, 0-30 feet; blue rock, 30-280 feet; 
sand and water. 280-315 feet. 



Well at Lock 3 (now Lock 6), Black Warrior River, Erie Landing, in 
•the N. W. quarter Section 16, Township 20, Range 3 E.; bored. by Kin- 
naird & Sample in 1903; depth, 520 feet; casing, 20 feet, 3-inch; first water 
at 300 feet, stood at -35 feet; second water, at 400 feet, stood at -8 feet; 
at 400 feet the water flowed over for two days; yield, 3 gallons per min- 
ute; temperature, 68° Record: Lime rock, 0-20 feet; blue rock, 20-300 
feet; alternating sand and blue rock, 300-400 feet; pink soapstone, 400-500 
feet. The last is probably Tuscaloosa formation, the first 400 feet being 
Eutaw sands and rock. 



WATERS OF Tin- CRETACEOUS. 167 

GREENSBORO AM) VICINITY. 

The city of Greensboro has several 4-inch wells about 432 
feet deej). situated in a depression about 48 feet below the level 
of the court-house. The water stands at -30 feet, and the ag- 
gregate yield of the wells by air lift is no gallons per minute. 
Mr. C. E. Waller states that in the borings ten water-bearing 
strata were pas'sed, indurated ledges about 10 feet apart being 
above and below the water-bearing sands. The formation 
throughout is Eutaw. The composition of the water from the 
city supply is as follows, the analysis being by Mr. Hodges : 

Analysis of water from wells of Greensboro city tvaterworks. 



Parts per million. 

Potassium (K) 5.1 

Sodium (Na) 24.9 

Magnesium (Mg) 13.1 

Calcium (Ca) 21.8 

Iron and alumina (Feo0 3 , A1.>0 3 ) 5.3 

Chlorine (CI) 60.4 

Sulphuric acid (S0 4 ) 4.8 

Carbonic acid (HCO s ) 95.6 

Silica (Si0 2 ) 4.6 

235.6 



Mr. William Withers states that borings have been made in 
this basin to depths of from 75 to 1,600 feet. The shallow 
wells furnish an ample domestic supply, while those from 500 
to 800 feet deep give abundant water for industrial, manufac- 
turing, and irrigatiuon purposes. 

J. M. P. Otts's well. Greensboro, in the S. W. quarter S. E. quarter 
Section 17, Township 20, Range 5 B.; bored by Morrison in 1903; depth, 
157 feet; casing, 36 feet, 3-inch; water stands at -7 feet. Record: Soil, 
0-23 feet; blue rock, 23-55 feet; sand and water, 55-115 feet; blue rock, 
115-157 feet. 

Blount & Ward's well, bored by Morrison in 1902; depth, 500 feet; 
casing, 3-inch; water stands at -13 feet; well has never been used. 
Record: Clay, 0-30 feet; blue rock. 30-300 feet; sand and thin strata of 
blue rock. 300-425 feet; pink soapstone, 425-500 feet. 

Cotton Oil Company's well, 300 yards from Blount & Ward well; bored 
by Morrison in 1902; depth, 500 feet; casing, 30 feet, 6-inch; water stands 
at -13 feet; reported to carry much sulphur; used in boilers at mill; 
gives no crust; supply reported inexhaustible. Record: Clay, 0-30 feet; 
blue rock, 30-300 feet; sand, with occasional strata of blue rock, 10 
inches to 3 feet thick, 300-500 feet. 

Lee Otts's well, on Jenkins place, about 2 1-2 miles southwest of Greens- 
boro, in the N. W. quarter Section 30, Township 20, Range 5 E.; bored 



168 details: coastal plain division. 

by Morrison in 1903; depth, 600 feet; casing, 3-inch; water stand at -7 
feet; well abandoned. Record: Sand, 0-22 feet; blue rock, 22-400 feet; 
pink soapstone, 400-600 feet. Water is from a stratum of sand in the 
blue rock. 

In the lower part of the county, west and southwest of 
Greensboro, in the prairie region, are to be found many of the 
old-time rich plantations. This region, as has been shown, 
is deficient in shallow-water supply. From the beginning re- 
course has' been had to artesian borings, and new wells are con- 
stantly being put down as necessity arises. The following re- 
cords will sliow how these borings are concentrated about the 
older settlements and plantations. 

Cheney Borden's well, 6 miles west of Greensboro; bored by Kinnaird 
& Sample in 1901; depth, 400 feet; diameter, 3 inches; water stands at 
-40 feet; used two months and abandoned. 

MILLWOOD AND VICINITY. 

Wiley Tunstall's wells: No. 1, in the S. E. quarter Section 35. Town- 
ship 20, Range 3 E., at Millwood, 300 yards northwest of the house, 
across pond; bored by Kinnaird & Sample in 1901; depth, 330 feet; casing, 
6-inch; flowing water obtained at 300 feet; original yield (estimated), 
40 gallons per minute; present yield, 30 gallons per minute, flowing 3 
feet above surface; temperature, 66°. Record: Soil, 0-40 feet; blue rock; 
40-300 feet; sand and water, 300-330 feet. No. 2, 400 yards north of house; 
bored by Kinnaird & Sample to 300 feet in 1901 and deepened to 500 feet 
in 1902; depth, 500 feet; casing, 6-inch; flow in 1902, 75 gallons per minute; 
temperature, 68°; reported to have mineral properties. Record: Soil, 
0-40 feet; blue rock, 40-240 feet; sand, water, etc., 240-500 feet. No. 3, 70 
yards northwest of mill house; bored by Kinnaird & Sample in 1902; 
depth, 500 feet; casing, 4 1-2 inch; flowing water at 260 feet, rising to 2 
feet above the ground; yield, 75 gallons per minute; temperature, 68°. 
Record. Soil, 0-50 feet; blue rock, 50-260 feet; sand and water, with thin 
strata of blue rock, 260-500 feet.. No. 4, 80 yards west of house; bored by 
Kinnaird & Sample in 1902; depth, 500 feet; casing, 4 1-2-inch; first flow- 
ing water at 260 feet; present yield, at 2 feet above the ground, .75 gal- 
lons per minute; temperature, 68° Record: Soil, 0-50 feet; blue rock, 
50-260 feet; sand and water, with thin strata of blue rock, 260-500 feet. 
No. 5, in the S. E. quarter N. vV. quarter Section 33, Township 20, Range 
4 E., on Jeffrey place (pasture well); bored by Kinnaird & Sample in 
1902; depth unknown; diameter 3 inches; present yield, 9 gallons per min- 
ute; temperature, 69°. No. 6, in the S. W. quarter S. E. quarter Section 
29, Township 20, Range 4 E., on Jeffrey place, near George Taylor's 
store, 3 miles east of Millwood; bored by Kinnaird & Sample in 1902; 
depth, 360 feet; casing, 3-inch; flowing water at 300 feet, rising to 2 feet 
above the ground; estimated original volume, 6 gallons per minute; 
present volume, 3 gallons per minute (much leakage); temperature, 70°.- 
No. 7, at Grindle Pond, 2 miles north of Millwood, in section 23, Town- 
ship 20, Range 3 E.; bored by Kinnaird & Sample in 1902; depth, 200 
feet; casing, 3-inch; flowing water at 120 feet; present yield, 38 gallons 
per minute at 2 feet above the ground; temperature, 66°. 



GEOLOGICAL SURVEY OF ALABAMA. UNDERGROUND WATER RESOURCES. PLATE XV. 




A. Well on Crassdale Plantation, (J. O. Banks), near Eutaw, Green County. 




B. Pickens Well, near Greensboro, Hale County. 



WATERS OF THE CRETACEOUS. .169 

Wells Nos. I to 4 of Colonel Tunstall at Millwood Landing, 
above described, have been recently bored to take the place of 
old wells which formerly supplied water for a mill. Some of 
the old wells are still in use, but are not included in the above 
notes. One large well on the river bank has lately been de- 
stroyed by the caving of the bank. Reports of the depths of 
the ante-bellum wells are generally exaggerated, as 1 is shown 
by recent borings in the same localities. 

Pickens well, about 2 miles southeast of Millwood, in the 
N. W. quarter N. E. quarter Section 6, Township 20, Range 
4 E., on the old Samuel Pickens place ; one of the largest wells 
in the State; diameter of casing, 71-4 inches; water rises in a 
solid stream 9 inches above the top oT the pipe ; estimated flow, 
850 gallons per minute; temperature, 72°. In the immediate 
vicinity of this well are four or five others of varying capacity, 
some of them extremely bold, others' weak. Xo reliable re- 
cords are obtainable, but it is reported that the wells have depths 
varying - from 450 to 850 feet, the former figure being probably 
nearer correct. PI. XV. B. shows the Pickens well in its pres- 
ent state. 

M. H. Murphy's wells: No. 1. 1 1-2 miles east of big Pickens well, 
in Section 5, Township 19, Range 4; bored by J. I. Hawk in 1903; depth, 
502 feet; casing. 2-inch; flow, 11 gallons per minute; temperature, 70° 
i>o. 2, (old well, cleaned out by Hawk), in the N. E. quarter S. E. quar- 
ter Section 8, Township 19. Range 4; depth, 497 feet; casing, 2-inch. 

Well at Lock 2 (5), in the S. W. quarter Section 25, Township 19, Range 
3 E. ; drilled in 1903; depth, 400 feet; casing, 3-inch; weak overflow from 
depth of 3C0 feet; estimated yield, 30 gallons per minute; temperature, 
67°. Record: Soil and clay. 0-20 feet; blue rock, 20-280 feet; sand with 
water, 280-400 feet. 

CEDABVILLE AND VICINITY. 

A. C. Jones's well, Cedarville, in the S. E. quarter ^ection 15, Township 
19, Range 4; old well, not flowing. 

Kelly Brothers' well, Cedarville. in the S. W. quarter S. W. quarter 
Section 15, Township 19, Range 4; bored by Ben Rainey about 1873; 
depth, about 275 feet; flow 4 gallons per minute; supply constant, water 
rises to 3 feet above the ground; temperature, 68°. 

Tom Ruffin's wells: No. 1, on O'Donnell place, 1 mile northwest of 
Cedarville; flow, 8 gallons per minute; temperature, 67°; old well. No. 
2, 200 yards north of No. 1; in decay, but still flows. No. 3, 1 1-4 miles 
northwest of Cedarville, in Section 1<5. Township 19, Range 4; flow, 5 
gallons per minute; water rises to 4 feet above the ground; temperature, 
67°. No. 4, 1 1-2 miles northwest of Cedarville, in Section 16, Township 
19, Range 4; no record. These wells are located about 2 miles southeast 



170 details: coastal plain division. 

of the big Pickens well. No. 5, Cedarville, in the N. W. quarter N. W. 
quarter, Section 32, Township 19, Range 4; flows 2 gallons per minute; 
temperature, 68°. 

A. B. Gewin's well, Cedarville, in the N. E. quarter N. E. quarter Sec- 
tion 32, Township 19, Range 4; does not overflow; windmill used; old well. 

Sledge & Leonard's well, Cedarville, in the N. W. quarter N. E. quar- 
ter Section 22, Township 19, Range 4; does not flow; pump used; water 
stands at -5 feet; temperature, 67° 

Sander's mill well, Cedarville, in the N. W. quarter N. E. quarter Sec- 
tion 22, Township 19, Range 4; water rises to 2 feet above the ground; 
flow, 2 1-2 gallons per minute. 

Peyton Agnew's well, 1 mile west of Cedarville, in the N. W. quarter 
N. E. quarter Section 21, Township 19, Range 4; old well; flow, 1 gallon 
per minute; temperature, 67°. 

Kelly Brothers' well, 1 1-2 miles southwest of Cedarville, in Section 
28, Township 19 Range 4; bored in 1902; depth, 175 feet; flow, 2 gallons per 
minute; temperature, 65°. 

WHITSITT AND VICINITY. 

Wells on Egypt place: No. 1. 1 1-2 miles west of Whitsitt, in the S. E. 
quarter S. E. quarter Section 13, Township 19, Range 4; flowing; in decay; 
temperature. 66°. No. 2, 2 1-2 miles west of Whitsitt, in the S. E. 
quarter S. E. quarter Section 13, Township 19, Range 4; estimated flow, 
10 gallons per minute; temperature, 66°. No. 3, 2 1-4 miles west of Whit- 
sitt, in the S. E. quarter S. E. quarter, Section 13, Township 19, Range 4; 
flow, 15 gallons per minute; temperature, 67°. No. 4, 2 1-4 miles west of 
Whitsitt, in the N. E. quarter N. E. quarter Section 24, Township 19, 
Range 4; bored by Ben Rainey in 1902; depth, 125 feet; flow, 1 1-2 gallons 
per minute; temperature, 67°; no further data obtainable. No. 5, 2 miles 
west of Whitsitt, in the N. E. quarter S. E. quarter Section 13, Township 
19, Range 4; flow, 1 1-2 gallons per minute; temperature, 66°. These are 
all old wells. 

"Wells on Knight place: No. 1, 3 1-2 miles south of Greensboro, near 
center of Section 7, Township 19, Range 5; flow, 6 gallons per minute; 
water level, 3 feet above the ground; temperature, 67° No. 2, in the S. E. 
quarter S. W. quarter Section 7, Township 19, Range 5; flow, 4 gallons 
per minute; temperature, 67 1-2°. No. 3, inthe S. E. quarter S. W. quar- 
ter Section 7, Township 19, Range 5; temperature, 66 1-2°; flows, but in 
decay. No. 4, in the S. E. quarter N. E. quarter Section 18, Township 
19, Range 5; flow, 4 gallons per minute; water level, 3 feet above the 
ground; temperature, 67°. No. 5, no record. These are old wells. 

Wells on Peck place: No. 1, in the N. W. quarter S. W. quarter Sec- 
tion 5, Township 19, Range 5; flow, 20 gallons per minute at 4 feet above 
the ground; temperature, 66°. No. 2 near center of Section 5, Township 
19, Range 5; flow, 5 gallons per minute; temperature, 66°. Both old wells. 

George Erwin's wells (old): No. 1, one-half mile west of Whitsitt, 
in the N. W. quarter S. E. quarter Section 20, Township 19, Range 5; 
flow, 1 gallon per minute; temperature, 71°. No. 2, one-half mile north 
of west of Whitsitt, in the N. E. quarter S. E. quarter Section 20, Town- 
ship 19, Range 5; does not flow. No. 3, one mile north of west from Whit- 
sitt, in the N. W. quarter N. W. quarter Section 20, Township 19, Range 
5; flow, 3 gallons per minute; temperature, 66°. 

Wells on Mrs. Tunstall's place: No. 1, one-half mile east of Whitsitt, 
in the -S. E. quarter S.W. quarter Section 21, Township 19, Range 5: 



WATERS OF TUK CRETACEOUS. 171 

flow, one-quarter gallon per minute; temperature, 67 1-2°. No. 2, 1 mile 
north of No. 1, in the N. E. quarter N. W. quarter Section 21, Township 
19. Range 5; flows one-quarter gallon per minute. Both old wells. 

Mrs. C. L. Karnegie's well, at Whitsitt, in the S. W. quarter S. W. quar- 
ter Section 21, Township 19, Range 5; old well; no longer flows. 

Well on Karnegie place, 1 1-2 miles south of Whitsitt; owned by Mr. 
White, of Newberne; flow, two-thhus of a gallon per minute;' tempera- 
ture, 66°. 

"Wells on "Long Farm" place, near center of Section 29, Township 
19; Range 5: No. 1. 1 mile southwest of Whitsitt; in decay; water stands 
at surface. No. 2, in decay. Both old wells. 

Wells on Harris Tinker place: No. 1, 1 mile south of Whitsitt, in the 
N. W. quarter S. W. quarter Section 28, Township 19, Range 5; flow, one- 
half gallon per minute; temperature, 67°. No. 2, 1 mile south of Whit- 
sitt, in the N. W. quarter S. W. quarter Section 28, Township 19, Range 
5; flow, one-half gallon per minute. No. 3, in the S. E. quarter N. W. 
quarter Section 28, Township 19, Range 5; well now in decay. No. 4, 
N. W. quarter S. W. quarter Section 28, Township 19, Range 5; in decay. 
No. 5, N. W. quarter S. W. quarter Section 28, Township 19, Range 5; 
flow, one-fifth of a gallon per minute; temperature, 67°. All these are 
old wells. 

Wells on Mrs. Mattie Croom's place, in Section 22, Township 19, Range 
5; two old wells that flow about two-thirds of a gallon per minute; 
temperature, 67°. 

Wells on Mauldin place: No. 1, 1 1-2 miles southeast of Whitsitt, in 
Section 27, Township 19, Range 5; flow, one-third of a gallon per minute; 
temperature, 67°. No. 2, 1 1-2 miles south of Whitsitt, in the N. W. 
quarter N. W. quarter Section 33, Township 19, Range 5; flow, one-half 
gallon per minute; temperature, 66°. Both old wells. 

NEWBERNE AND VICINITY. 

Well on Irvin plantation, 2 1-2 miles northeast of Newberne; bored by 
J. I. Hawk in 1899; depth, 300 feet; water stands at -27 feet; quality good. 
No blue rock encountered; well starts in the Selma chalk; water supply 
from Eutaw sands. 

M. S. Heron's wells: No. 1, one-half mile northwest of Newberne, in 
the N. W. quarter S. W. quarter Section 24, Township 19, Range 5; 
bored by Hawk in 1900; depth, 300 feet; casing, 4-inch; water stands at 
-35 feet; temperature, 67°. No. 2, 1 mile northwest of Newberne; bored 
in 1S96; in the S. E. quarter Section 14, Township 19, Range 5; depth, 350 
feet; does not flow. 

R. L. Bennett's wells: No. 1, near Newberne, in the N. E. quarter S. W. 
quarter Section 24. Township 19. Range 5; bored by Andrew Clark in 
1878; depth. 425 feet; cased 250 feet with 5-inch casing; first water, at 105 
feet, stood at -40 feet; second water at 165 feet, stood at ? feet; third 
water, at 225 feet, stood at -16 feet; fourth water, at 350 feet, stood at 
-30 feet. No. 2, three-quarters of a mile west of Newberne, in the N. W. 
quarter Section 24, Township 19. Range 5; bored by Andrew Clark in 
1878; depth, 50 feet; flows 1-inch stream. 

A. E. Walker's well, Newberne, in the N. E. quarter N. W. quarter 
Section 25. Township 19, Range 5; bored by Hawk in 1903; depth, 300 feet. 

P. S. Morrisette's well, Newberne, in the S. E. quarter N. W. quarter 
Section 25, Township 19; Range 5; bored by Hawk in 1903; depth, 300 
feet. 



172 details: coastal plain division. 

Well on F. S. Morrisette plantation, where P. Morrisette lives; bored 
by Hawk in August, 1903; depth, 400 feet; casing, 20 feet 4-inch; first 
water at 300 feet, rose 2 feet above surface; second water, at 400 feet, 
rises 10 feet above surface; depth to principal water supply, 400 feet; 
original flow, 10 gallons per minute; depth to blue rock, 18 feet; thickness 
of blue rock, 250 feet. 

Well of Farmers' Gin and Warehouse Company, bored by Hawk; 
depth, 485 feet; flow, 3 gallons per minute; starts in Selma chalk; water 
in Eutaw sands. 

W. H. Landers's well, in the S. B. quarter S. W. quarter Section 24, 
Townsend 19, Range 5; bored by Hawk in 1903; depth, 300 feet; casing, 
20 feet, 3-inch; first water, at 165 feet, stood at -42 feet; second water, 
at 300 feet, at -30 feet. Record same as J. H. Turpin's well below. 

Dr. J. Huggins reports that he has a well that does not overflow; water 
stands at -23 feet; impregnated with iron, sulphur, and lime. He also 
reports the "Duffin saline well," in Newberne, formerly owned by his 
father, now the property of S. Hardenbergh. This is an old well; the 
water was much used before the war, being thought good for indigestion. 
The analysis, by Mr. Hodges, is as follows: 

Analysis of icater from S. Harclenbergh's well, Newberne. 



Parts per million. 

Potassium (K) 24.8 

Sodium (Na) 266.0 

Magnesium (Mg) 39. 6 

Calcium (Ca) 589.2 

Iron and alumina (Fe 2 O s , ALQ 3 ) 12.2 

Chlorine (CD 720.1 

Sulphuric acid (SO*) 760.4 

Carbonic acid (HCO s ) 528.6 

Silica (Si0 2 ) 43.4 

2984.3 



Dr. Huggins says there are four very large flowing wells near New- 
berne which yield about 250 gallons per minute. He estimates about 200 
artesian wells about Newberne, most of them yielding from 1 to 20 
gallons per minute. 

J. J. Hogue's well, Newberne, 400 yards southwest of post-office, in 
the N. W. quarter S. W. quarter Section 25, Township 19, Range 5; 
bored by Hawk in 1900; depth, 300 feet. Record same as that of J. H. 
Turpin.s well. 

J. H. Turpin's well, 1 mile from Newburne, in the S. W. quarter Sec- 
tion 25, Township 19, Range 5; bored by Hawk in 1901; depth, 350 feet; 
casing, 20 feet, 4-inch-; first water at 110 feet; second water at 320 feet; 
overflows; original flow, 16 gallons per minute; temperature, 67°. 



WATERS OF THE CRETACEOUS. 173 

Record of J. H. Turpin's well, 1 mile from Newberne. 



Feet. 

Clay 0— 20 

Blue rock 20— 95 

Sand and soapstone 95 — 105 

Hani rock 105 — 107 

Soapstone 107 — 167 

[ I ard rock 107 — 169 

Soapstone 169 — 250 

Sand and soapstone 250 — 300 

Soapstone 300 — 350 



Andrew J. Moore's wells: No. 1, at residence, near Newberne; bored 
by Hawk in 1903;depth, 500 feet; cased witb 2- and 4-inch pipe; water 
stands at -20 feet; first water at 250 feet; second water at 340 feet; third 
water at 420 feet; fourth water at 500 feet; thickness of blue rock, 175 
feet; depth to blue rock, 20 feet. No. 2, in lot, 2 1-2 miles south of New- 
berne; bored by Hawk in 1900; depth, 5C0 feet; flow, 6 gallons per minute; 
blue rock was encountered at 12 feet and. continued to 137 feet; well 
starts in Selma chalk; water supply from Eutaw sands. No. 3, bored 
by Hawk in 1903. 

D. L. Moore's wells, bored by J. I. Hawk: No. 1, depth 300 feet; flow, 
28 gallons per minute. No. 2, depth. 410 feet; flow 35 gallons per minute. 

Pollard Brothers' well, bored by J. I. Hawk in 1903; depth, probably 
300 feet or more; water stands at -18 feet; blue rock at 22 feet, 80 feet 
thick. 

W. R. Tubbs's well, bored by J. I. Hawk in 1900; depth, 300 feet; water 
stands at -28 feet; blue rock at 20 feet, 85 feet thick. 

R. A. White's well, bored by J. I. Hawk in 1900; depth, 300 feet; water 
stands at -22 feet; blue rock at 20 feet, 85 feet thick. 

R. A. White & Co.'s well, at store, one-quarter of a mile north of 
depot, Newberne; bored by Hawk in June, 1903; depth, 300 feet; casing, 
2u feet, 4-inch; first water at 165 feet, rising to -40 feet; second water 
at 285 feet, rising to -30 feet; depth to principal water supply, 285 feet; 
pump used; depth to blue rock, 19 feet; thickness of blue rock, 85 feet. 

Well at Newberne (owner unknown), reported depth, 475 feet; water 
rises to 4 feet above the ground; flows 30 gallons per minute; blue rock 
8u feet thick. 

W. P. Nelson's well. 2 1-2 miles southwest of Newberne; bored by Hawk; 
depth, 500 feet; flow, 8 gallons per minute; blue rock at 20 feet, 200 feet 
thick. 

Carter Washington's well, in lot, 4 miles southwest of Newberne; 
bored by Hawk in August. 1903; depth. 400 feet; casing 20 feet, 4-inch; 
first water at 300 feet, rising to -2 feet; second water at 400 feet, rising 
to 5 feet above the ground; depth to principal supply, 400 feet; flow 6 
gallons per minute; depth to blue rock, 10 feet; thickness of blue rock, 
240 feet. 

Ned Pickens's well, 4 1-2 miles southwest of Newberne; bored in 
October, 1900, by J. I. Hawk; depth, 300 feet; diameter, 4 inches; first 
water, at 200 feet, flowed 2 feet above surface; second water, at 300 
feet, flowed 12 feet above surface; depth to principal water supply. 260 
feet; original flow, 15 gallons per minute; depth to blue rock, 16 feet. 



174 details: coastal plain division. 

SUNSHINE. 

Well (owner unknown), reported to have been bored by J. I. Hawk to a 
depth of 300 feet; flow, 12 gallons per minute; blue rock at 18 feet, 
thickness 185 feet. . 

LANEVILLE AND VICINITY. 

I. F. Lewis's well, 2 miles southwest of Laneville; bored by Hawk in 
June, 1901; depth, 710 feet; casing, 375 feet, 2-inch and 4-inch; first water, 
at 350 feet, rose to -18 feet; depth to principal water supply, 690 feet; 
overflows; depth to blue rock, 16 feet; thickness of blue rock, 325 feet. 

Garber Brothers' (new) wells: No. 1, 1 mile south of Laneville; flow, 
4 gallons per minute; rises to 2 feet above the ground; temperature, 74°. 
No. 2, located one-half mile north of No. 1; flows one-half gallon per min- 
ute; rises to 2 feet above the ground; temperature, 73°. No. 3, flows 10 
gallons per minute; stands at surface; temperature, 66°. No. 4, 1 mile 
west of No. 3; flow, '8 gallons per minute; rises to 2 feet above the ground; 
temperature, 66°. 

Well on Rugh place, 3 miles northwest of Laneville, owned by W. B. 
Inge, of Greensboro; bored by Hawk in July, 1901; depth, 400 feet; casing 
18 feet, 4-inch; first water at 250 feet, rising 2 feet above surface; second 
water at 390 feet, rising 12 feet above surface; depth to principal water 
supply, 390 feet; original flow, 15 gallons per minute; depth to blue rock, 
16 feet; thickness of blue rock, 200 feet. 

Wells on Hermitage place, 4 miles north of Laneville, owned by Lewis; 
4 old wells. 

Wells on "Bleak House place," owned by Mrs. Ivey Lewis estate: No. 
1, near center of Section 12, Township 18, Range 4; flow, 1 1-2 gallons per 
minute; rises to 2 feet above ground; temperature, 68°. No. 2, in the N. 
W. quarter S. W. quarter Section 7, Township IS, Range 5; flow, 4 gal- 
lons per minute; rises to 3 feet above the ground; temperature, 69°. 
No. 3, in the N. E. quarter S. E. quarter Section 12, Township 18, Rang» 
4; flow, 3 gallons per minute; rises to 3 feet above the ground; tempera- 
ture, 69°. No. 4, in the S. E. quarter bection 12, Township 18, Range 4; 
flow, 4 gallons per minute; rises to 5 feet above the ground; temperature, 
67° No. 5, in the S. W. quarter S. E. quarter Section 12, Township 18, 
Range 4; flows weak stream. These are au old wells. 

GALLION AND VICINITY. 

Wells on "Oak Grove place," 3 or 4 miles northeast of Gallion, owned 
by Ivey P. Lewis, formerly owned by C. W. Collins: No. 1, in the N. E. 
quarter Section 15, Township 18, Range 4; depth, 200 feet; casing, 3-inch; 
flow, 1 gallon per minute; water rises to 4 feet above the ground; tem- 
perature, 68°. No. 2, in the S. E. quarter Section 11, Township 18, Range 
4; flow, 5 gallons per minute; temperature, 69°. No. 3, S. E. quarter Sec- 
tion 11, Township 18, Range 4; no record. No. 4, N. E. quarter Section 
15, Township 18, Range 4; depth, 700 feet; casing, 3-inch; flow, one-quarter 
of a gallon per minute; water rises to 5 feet above ground; temperature, 
70°. No. 5, in the N. E. quarter, Section 15, Township 18, Range 4; depth 
900 feet; casing, 3-inch; flow, 1 gallon per minute; water rises to 5 feet 
above the ground; temperature, 70°. No. 6, in the S. W. quarter Section 
10, Township 18, Range 4; flow, one-half of a gallon per minute; water 



WATERS OF THE CRETACEOUS. 175 

rises to 3 feet above the ground; temperature, 68°. No 7, in the N. W. 
quarter Section 14, Township 18; Range 4; flow, 1 gallon per minute; 
temperature, 70°. No. 8. in the S. E. quarter Section pi. Township ]S, 
Range 4; flow, 2 gallons per minute; temperature, 70°. 

Well on "Simon Tract place," owned by Mrs. Dr. Browder, in Section 
9, Township 18, Range 4; flow, one-third gallon per minute; temperature, 
6S°. 

Mrs. Collins's wells (old), in the S. W. quarter N. E. quarter Section 

17. Township 18, Range 4: No. 1, flow, 4u gallons per minute; water rises 
to S feet above the ground, temperature, 72°. Two other wells, one-quar- 
ter and one-half mile North of No. 1. flowing 1 or 2 gallons per minute. 

C. W. Collins's well, in the N. E. quarter S. E. quarter Section 17. 
Township 18. Range 4; old well; flow, one-half gallon per minute; water 
rises to 3 feet above the ground; temperature, 6S 1-2°. 

Mrs. Julian Collins's well, 2 miles northeast of Gallion. in the S. W. 
quarter Section 19, Township 18, Range 4; old well; flows good stream. 

C. W. Collins's wells, 1 1-2 to 2 miles northeast of Gallion (old wells): 
No 1, at house, in the S. W. quarter S. W. quarter Section 27, Township 

18, Range 4; depth, 1200 feet; formerly flowed; water now stands at -8 
feet. No. 2, at house; bored in 1891; depth, 1500 feet; overflow from about 
750 feet; thickness of lime rock, 250 feet; at 1250 feet encountered red 
stratum. No. 3, 3 miles northeast from Gallion, in Section 22, Township 
18, Range 4; depth, 600 or 700 feet; flow. 5 gallons per minute; temperature, 
72° ; thickness of lime rock, 250 feet. No. 4. 3 miles northeast of Gallion, 
in Section 23, Township 18, Range 4; uepth, 600 or 700 feet; flow, 7 1-2 
gallons per minute; water rises to 4 feet above the surface; temperature, 
71°. No. 5, in Section 15, Township 18, Range 4; depth, 600 or 700 feet; 
flow, 2 gallons per minute; temperature, 69°. 

B. M. Allen's wells, 3 miles east of Gallion; two old wells, no longer 
flowing. Mr. Allen has recently had other wells bored of which records 
have not been obtained. 

rtTells on Dunlap place: No. 1, 1 1-2 miles north of Prairieville; flow, 
20 gallons per minute. No. 2, 1 mile southwest of No. 1; flow, 2 gallons 
per minute. 

FAUNSDALE AND VICINITY. 

Well on Madden place, 3 miles north of Faunsdaie, owned by Garber 
Brothers; flow, 1 gallon per minute; temperature, 69°. 

Wells on Drake place: No. 1, 3 miles north of Faunsdaie; flow one- 
quarter gallon per minute; rises to 2 feet above ground; temperature, 
69°. No. 2, one-quarter mile southwest of No. 1; flow, one-half gallon 
per minute; rises to 2 feet above ground. No. 3, one-quarter mile south- 
west of No. 1; flow, 1 gallon per minute; water stands at surface. No. 
4, 200 yards east of No. 1; flow, 30 gallons per minute; temperature, 75°; 
recently cleaned. 

Wells on Croom place, owned by J. H. Minge (old wells): No. 1, 3 
miles north of Faunsdaie; flow, 1 1-3 gaiions per minute; rises to 4 feet 
above the ground; temperature, 70°. No. 2, one-quarter mile east of No. 
1; flow, one-quarter gallon per minute; rises to 2 feet abovetheground; 
temperature, 70°. No. 3, 1 mile south of No. 1; 1 gallon per minute; 
rises to 3 feet above the ground; temperature, 69°. 

Well of Mr. London, of Birmingham, 6 miles south of Newberne, 
and about same distance north of Faunsdaie; bored by Kinnaird & Sample 
in 1902; depth, 500 feet; 3-inch casing; overflowing water obtained at a 



176 DETAILS : COASTAL, PLAIN DIVISION. 

depth cu 500 feet after three days; flow, 5 gallons per minute; temperature, 
68°. Record: Soil 0-S feet; blue rock with occasional strata of sand, 
8-500 feet. 



PERRY COUNTY. 
Shallow Watees. 

On account of its great extent from north to' south, Perry 
County embraces within its borders all four of the Cretaceous 
formations and exhibits in consequence much variety in its to- 
pography and soils. The northeastern part down nearly to the 
latitude of Marion is underlain by the Tuscaloosa formation, 
cross-bedded sands of many colors, with strata of massive or 
joint clay of mottled red, purple, brown, and gray colors. In 
all this section the country is somewhat hilly, and the surface 
soils, being formed either by the sandy strata of the Tusca- 
loosa or the equally sandy beds of the overlying Lafayette, are 
well suited for absorbing and transmitting the waters which 
fall upon them. Generally, therefore, in this section there is 
no dearth of water to be had from wells and hillside springs. 
Many of the wells, however, have a tendency to go partially 
dry in the winter season. 

The Eutaw formation, composed of sands and laminated 
clays, makes a narrow belt between the Tuscaloosa and the 
Selma chalk. Very nearly the same conditions of topography 
and soils prevail here as in the Tuscaloosa area, and open wells 
and springs are numerous. 

In the limestone territory, on the other hand, shallow waters 
are deficient and deep wells correspondingly more numerous. 

Some of the springs in the Tuscaloosa and Eutaw terranes 
are well known, and a few of them may be mentioned : The 
Popular Spring, near the old town of Hamburg, 5 miles south 
of Marion, is a cold spring boiling up through the sands; half 
a mile southeast of this is a similar spring, the Norman ; 8 
miles southeast of Marion, on the Fikes place, 1 mile from the 
bridge, is a spring, small but constant in all seasons, tempera- 
ture, 66° ; 12 miles a little east of south of Marion, is' the 
Haynesworth Spring of chalybeate water; 13 miles west of Ma- 
rion is Dr. W. T. Downey's sulphur spring; 11 miles west •■ f 
Marion on R. M. Foster's place, are several springs; in the 



WATERS Ol< THE CRETACEOUS. 177 

corporate limits of Marion is the Magnesia Spring, on the Per- 
kins place; 3 1-2 miles east of Marion on the road to Sprott, are 
the Clinton Springs which comprise several springs of sulphur 
and iron waters; 4 1-2 miles due east of Marion are the Bur- 
roughs' Springs, of mineral quality, some of them chalybeate; 
half a mile due north of Burroughs are several chalybeate 
springs ; 5 miles east of Marion in sec. 26. T. 20, R. 8, is C. YV. 
Ford's spring, strong of iron and formerly much used by 
Marion people. 

Artesian Waters. 

The Tuscaloosa and Eutaw sands are in this county, as else- 
where, the water-bearing sands of the artesian wells. Notwith- 
standing the fact that the territory of these formations is fairly 
well supplied supplied with shallow wells, the records show 
also a number. of artesian wells here. 

WELLS IN THE TUSCALOOSA FORMATION. 

The six wells recorded below are located on the outcrop of 
the Tuscaloosa in the northern and northeastern parts of the 
county, and obtain water from that formation. 

Well on Hornbuckle place, owned by H. A. Peters, near LeVert, in the 
S. E. quarter N. E. Quarter Section 34, Township 21, Range 8; flow, 155 
gallons per minute; water rises to 5 feet above the ground; 6-inch casing; 
temperature, 65°. This well was bored over 40 years ago, about the same 
time as the Sprott well No. 3. There were a number of these old wells 
in the vicinity, but all have stopped flowing except these two. 

T. M. Wallace's well, 8 miles northeast of Marion, in the N. W. quarter 
Section 14 or N. E. quarter Section 15, Township 20. Range 8; bored by 
a negro in 1898; depth, 250 feet; cased to bottom with 5, 4, and 3 1-2 inch 
casing; first overflow at 100 feet; second overflow at 150 feet, bold stream; 
present flow, one-half gallon per minute; temperature, 65 1-2°. No hard 
rock, but principally sand, with one or two strata of blue rock. Partly 
bituminized logs were encountered between 50 and 100 feet. 

Lovelace well, 6 miles a little north of east of Marion; old well; for- 
merly overflowed; water now rises just to the surface; used as a kind 
of cistern. 

Sprott wells: No. 1. at house, in the N. W. quarter N. W. quarter Sec- 
tion 31. Township 20, Range 9; bored by hand in 1886; depth, 150 feet; 
cased to bottom with 4 and 6 inch casing; temperature, 66°. At 150 feet 
water rose 2 feet above surface; on penetrating a thin stratum of rock 
at this depth, the water rushed up with great violence, flowing 60 gal- 
lons per minute. Record: Sand, 0-30 feet; Tuscaloosa formation, 30-150 
feet; then a few inches of hard rock. No. 2, at quarter, 1 mile south of 
No. 1, in the N. W. quarter N. W. quarter Section 6, Township 19, Range 
12 



178 details: coastal plain division. 

9 E. ; bored by hand in 1895; depth, 150 feet; cased to bottom with 4 and 
6 inch pipe; flow, 1 gallon per minute; temperature, 66°. Record: Sand, 
0-30 feet; Tuscaloosa formation. 30-150 feet. No. 3, on Wallace place, 
3 miles nearly south of No. 1, in the S. W. quarter Section 1, Township 
19, Range 8; very old well; depth, 150 feet; flow, 12 gallons per minute, 
originally much stronger; recently cased to bottom with 4-inch casing; 
temperature, 65°. Record: Sand, 0-30 feet; Tuscaloosa formation, 30-150 
feet. 

WELLS IN THE EUTAW FORMATION. 

On the Eutaw outcrop as on the Tuscaloosa, bored wells 
are not so numerous as in the region of the Selma chalk, but 
a few wells are recorded about Marion and to the southeast 
near Radfordville and .Felix. 

MARION AND VICINITY. 

Town well, Marion, in the E. half Section 12, Township 19, Range 7; 
bored in 1898; depth, 650 feet; 6-inch casing; water stands at -150 feet. 

Well at old Ike Underwood place, 6 miles southwest of Marion, in the 
N. W. quarter Section 28, Township 19, Range 7; flow, 2 gallons per min- 
ute; temperature, 66°. 

Well on Ed. Craig place; old well; flows very weak stream. 

Peyton Tutwiler's wells (old): No. 1, in the S. W. quarter Section 16 
or 17, Township 19, Range 7; 5 miles west of Marion; flow, 1 gallon per 
minute; temperature, 66°. No. 2, one-half mile west of No. 1; estimated 
flow, 10 gallons per minute; temperature, 66°. Nos. 3 and 4 are in decay. 

OLD HAMBURG. 

In and around the town of old Hamburg, close to the contact 
of the Eutaw with the chalk foimation, but on the former, aie 
many old wells yielding bold streams of fine drinking water. 
As the town has gone down, many of these old wells have 
fallen into disuse. 

RADFORDVILLE. 

J. S. Alexander's wells, near Radfordville: No. 1, in Section 32, Town- 
ship 19, Range 9; diameter, 8 inches; flows IS gallons per minute; water 
rises to 4 feet above the ground; temperature, 66°; tastes strong of iron. 
No. 2, in the N. E. quarter N. E. quarter Section 6, Township 18, Range 
9; bored about 1859; depth 250 feet; 8-inch casing; original flow, 35 gallons 
per minute at 4 feet above the ground; present flow, 50 or 60 gallons per 
minute at surface; temperature, 66°; tastes strong of iron. 

W. B. Alexander's wells, near Radfordville: No. 1, one-half mile east 
from J. S. Alexander's well No. 1; depth, 250 to 300 feet; 8-inch casing; 
estimated flow, 50 gallons per minute, in decay; temperature, 67°; tastes 
strong of iron. No. 2, bored by an old negro in 1897; depth, 150 feet; 
casing 50 feet, 4-inch; first water at 150 feet; flow, 20 gallons per minute; 
water rises to 4 feet above the ground. 



WATliUS 01/ THE CRETACEOUS. 179 

FELIX AND VICINITY. 

Walter Smith's well, near Felix; bored by W. Suttle in 1903; depth, 210 
feet, 4-inch casing; first water at 210 feet; flow. 12 gallons per minute; 
water rises to 4 feet above the ground; temperature, 66°. 

Wells on Suttle & Jones plantation, near Felix: No. 1, at Mr. Suttle's 
house, in the northeast corner of the N. E. quarter S. W. quarter Sec- 
tion 1G, Township IS, Range 9; bored in December 1902, by Mr. Suttle: 
depth, 220 feet; casing, 40 feet, 4-inch; first water at 100 feet, overflowed; 
third water at 220 feet, flow, 12 gallons per minute; temperature, G7 Q . 
Record: Clay, 0-16 feet; gravel. 16-18 feet; clay, 18-35 feet; blue rock, 
35-100 feet; successive layers of white and black sand and some sand rock, 
100-220 feet. Water tastes very strong of"iron. No. 2, 200 yards north of 
No. 1, at gin, in the S. E. quarter N. W. quarter Section 16, Township 
18, Range 9; bored in 1898 by Pat Gilmore; depth, 198 feet; casing, 32 feet, 
4-inch; flow, 8 gallons per minute; temperature, 67°. No. 3, 2 miles west 
of north of No. 1, at fork of roads near Edwards place, in the N. W. 
quarter N. E. quarter Section 8, Township 18, Range 9; bored by Suttle 
in 1S97; depth, 96 feet; casing, 4-inch; record same as No. 1. No. 4, 2 
miles west of north from No. 1, in the N. W. quarter N. W. quarter Sec- 
tion 8. Township 18, Range 9; bored by Suttle in 1903; depth, ISO feet; 
casing, 30 feet, 4-inch; first water at 100 feet; second water at 180 feet; 
both overflowed; yield, 9 gallons per minute; temperature, 66°. No. 5. 
2 1-2 miles northwest of No. 1, in the center of the N t E. quarter Sec- 
tion 7, Township IS, Range 9; bored by Suttie in 1903; depth, 186 feet; 
casing, 35 feet, 4-inch; first water at 100 feet; second water at 186 feet; 
both overflowed; estimated yield, 11 gallons per minute; temperature, 
66°; record same as No. 1. No. 6, 1 mile west of north of No. 1, at 
Goshen place, in the center of the S. E. quarter Section 8, Township 18, 
Range 9; in every particular about the same as No. 1. No. 7, 2 miles 
west of north of No. 1; old well at W. S. Suttle' s residence, Edwards 
place, in the N. E. quarter N. W. quarter Section 8, Township 18, Range 
9; bored about 1S52; depth, 225 feet; diameter 6 inches; estimated flow, 
25 gallons per minute; temperature, 66°. Nos. 8 to 14, all within 3 miles 
of Felix, are old wells bored about 1850; casing, 4 and 6 inch; some are 
rather weak now, but all were formerly good strong wells: 

No. 8, on Vaughn place, in the N. W. quarter N. W. quarter Section 
9, Township IS, Range 9; 

No. 9, on Vanderslice place, in the N. W. quarter N. W. quarter Section 
21, Township 18, Range 9; 

No. 10, on Vanderslice place, in the S. E. quarter N. E. quarter Section 
20, Township 18, Range 9; 

No. 11, on Swift place, in the S. E. quarter S. E. quarter Section 28. 
Township 18, Range 9; 

No. 12, on Cooper place, in the N. W. quarter S. E. quarter Section 35, 
Township 18, Range 9; 

Nos. 13 and 14, on Davis place, in the N. W. quarter N. E. quarter, Sec- 
tion 2, Township 17, Range 9. 



WELLS IN THE SELMA CHALK. 

Most of the bored wells are naturally found in the relatively 
small area of the Selma chalk in the southwestern part of the 



180 details: coastal plain division. 

county. These wells get their supply generally from the Eutaw 
sands, the depth to which increases' southward and southwest- 
ward. 

UNIONTOWN AND VICINITY. 

The deepest of the wells on the Selma chalk is at Uniontown, 
which is also the southernmost point from which wells are 
recorded in Perry County. The altitude of Uniontown is 
286 feet, and the water stands at -120 feet. Depth of well 
(reported by the mayor in 1898), 1195 feet; diameter, 8 
inches ; water comes from the second horizon at 870 feet ; 
raised by air-lift; volume, 300 gallons per minute; supply seems 
inexhaustible ; temperature, 79° ; the quality of the water, good, 
onlyi78.o parts per million of dissolved solids; supply ample 
for the present needs of the town - . 

J. C. Welch's well, reported in 1898; depth, 895 feet; 8-inch casing to 
bottom; water stands at -125 feet; temperature, about 68°. 

G. D. Stollenwerck's well, 3 1-2 miles north of Uniontown; bored by 
Hawk in September, 1903; depth, 590 feet; casing, 275 feet, 2 and 4 inch; 
first water at 400 feet; second water, at 540 feet, stands at -60 feet; 
depth to principal supply, 550 feet; pump used; depth to blue rock, 20 
feet; thickness of blue rock, 350 feet. 

G. B. Johnston's well, 10 miles south of Uniontown; bored by J. I.- Hawk 
in 1904; depth, 875 feet; diameter, 4 and 3 inches; depth to principal supply, 
855 feet; water stands at -40 feet; yield, 10 gallons per minute with pump; 
water stratum at 175 feet. 

SCOTTS STATION. 

Howze Scott's wells, Scotts Station; 5 old, nonflowing wells; water 
stands at from 3 to 30 feet from surface, as it does in all the wells in 
this vicinity; age of wells not known; depth generally supposed to be 
from 85 to 300 feet. 

A. B. Gewin's well, Scotts Station, 300 yards northwest of station; depth, 
62 feet; casing, 18 feet, 4-inch. 

W. A. Thigpen's well, 3 miles south of Scotts Station; bored by a negro 
in 1896; depth, 100 feet; casing, 18 feet. 4-inch. 

SOUTHWARD FROM MARION. 

Wells on Billingsley place: No. 1, in the N. half of N. half Section 5, 
Township 18, Range 7, 7 miles southwest of Marion; in decay, flow de- 
creasing. No. 2, in the N. half Section 5, Township 18. Range 7; esti- 
mated flow, 1 gallon per minute; temperature, 66°. Nos. 3, 4 and 5 are de- 
creasing in flow; no other data. 

J. C. Tidmore's wells: No. 1, 8 miles south of Marion, on Lee place, 
in Section 28, Township 18, Range 8 B.; depth, 135 feet; bored with 4-inch 



WATERS OF TIIK CRETACEOUS. 181 

auger. Record: Soil, 0-20 feet; blue rock at 22 feet. No. 2, one-quarter 
mile from No. l. yields water of a dark color, not drinkable. No. 3, 
1 mile from No. 1. in the same hollow, yields water similar to No. 2, but 
not so bad. The character of the water from well No. 1 above is shown 
by the following analysis, by Mr. Hodges: 

Analysis of water from Tidmore well No. 1. 8 miles .south of Minion. 

Parts pei' million. 

Potassium (K) 11.3 

Sodium (Na) 177.fi 

Magnesium (Mg) 85.2 

Calcium (Ca ) 857.6 

Iron and Alumina (Fe-.0 3 .AloC-,~) 16. S 

Chlorine (CI) 661.1 

Sulphuric acid (SO,) 1448.5 

Carbonic acid (HCO a ) 546.5 

Silica (Si0 2 ) 54.4 

3859.0 



HAMBURG STATION AND VICINITY. 

J. T. Fitzgerald's wells (old), on plantation at Hamburg station: No. 
1. 1 mile southwest of Hamburg, in the S. E. quarter Section 19, Town- 
ship 18. Range 8; flow, three-quarter gallons per minute; temperature. 
66°. No. 2. 1 1-2 miles west of Hamburg, in the N. W. quarter S. E. qua- 
ter Section 19. Township 18. Range 8; flow. 1 1-2 gallons per minute; 
water rises to 2 feet above the ground; temperature, 66°. No. 3. 2 miles 
southwest of Hamburg, in the N. W. quarter Section 30, Township 18. 
Range 8; flow, 1 gallon per minute: temperature. 66°. No. 4. 2 miles south- 
west of Hamburg, in the N. W. quarter Section 30. Township IS, Range 8; 
flow. 2 gallons per minute; temperature, 66°. Nos. 5 and 6 are in decay 
and decreasing in flow. 

J. S. Blackmail's well, 2 1-2 miles southwest of Hamburg, in the W. 
half N. W. quarter Section 30, Township 18, Range 8; flow, 2 gallons per 
minute; temperature, 66°. 

R. B. Wallace's wells (old): No. 1. 2 miles southwest of Hamburg, in 
the S. W. quarter Section 29, Township IS. Range 8: flow, one-quarter 
gallon per minute; temperature, 66°. No. 2, 2 1-2 miles southwest of 
Hamburg; flow. 3 gallons per minute; water rises to 2 feet above the 
ground; temperature, 65°. No. 3, no longer flows; water stands at -40 
feet; pump used. 

Wells of Jones & Stewart, of Marion: No. 1, 3 miles west of south nf 
Hamburg, in Section 31. Township IS. Range 8; water stands at -5 feet.. 
No. 2, one-fourth mile north of No. 1; does not flow; water stands at 
-5 feet. No. 3, one-half mile west of No. 1, flow, 1 1-2 gallons per minute; 
temperature, 66°. No. 4, 1 1-4 miles west of No. 1; flow, 1 gallon per min- 
ute; temperature, 66°. No. 5, 1 1-4 miles west of No. 1; flow, 2 gallons 
per minute; temperature, 66°. These are all old wells. 

B. Tubbs and R. Tubbs each has an old, nonflowing well, 10 miles south 
of Marion. No information obtainable. 

Judge Shivers's well, on Tarrant place. 11 miles south of Marion; non- 
flowing. 

Well of Mrs. McCarroll, of Marion, 4 miles southwest of Hamburg, In 
the N. W. quarter Section 5, Township 17, Range S; flow. 5 gallons per 
minute; temperature, 67°. 



182 details: coastal plain division. 

MARION JUNCTION AND VICINITY. 

Many of the wells in this' vicinity, north and northeast of 
Marion Junction, are close to the county line, and there is 
occasionally some uncertainty as to whether they should be 
credited to Dallas or Perry County. Where the locations are 
given above in Township 17, Range 9, it would seem that they 
should come under Dallas, though the best information obtain- 
able credits them to Perry. It is therefore quite probable that 
the records of localities by the land numbers may be at fault. 

Mrs. Chisholm's well, 5 miles northeast of Marion Junction, in the S. B. 
quarter N. B. quarter Section 6, Township 17, Range 9, 150 yards from 
County line; flow, 1 gallon per minute; temperature, 69°; old well. 

Gordon Chisholm's well, 4 miles northeast of Marion Junction, at mill, 
in the N. E. quarter N. W. quarter Section 5, Township 17, Range 9; 
old well; estimated flow, 12 gallons per minute; water rises to 3 feet above 
the ground; temperature, 68 1-2°. 

Johnny Chisholm's wells: No. 1, 4 miles northeast of Marion Junction., 
adjoining Gordon Chisholm's place on the west; old well; flow, one-half 
gallon per minute; water rises to 1 foot above the ground; temperature, 
68°. No. 2, one-quarter mile east of No. 1; new well; bored by Patrick 
Gilmore in 1898; depth, 70 feet; flow, constant, 1 1-2 gallons per minute; 
temperature, 66°. This well is located about 2 miles from the limestone 
belt. Record: Blue rock, 0-69 feet; hard rock, water, 69-70 feet. 

Brown well, 150 yards from county line, one-quarter mile east of 
Mrs. Chisholm's well; flow, one-quarter gallon per minute; temperature, 
66°; old well. 

Sallie White's wells (old): No. 1, 5 1-2 miles northeast of Marion Junc- 
tion, just beyond the bridge; estimated flow, 5 gallons per minute; water 
rises to 2 feet above the ground. No. 2, one-quarter mile east of No. 1, 
on south side of road from Marion Junction to Selma; flows 10 gallons 
per minute; temperature, 67°. 

Well of W. J. & B. T. Gilmer, 3 1-2 miles Northeast of Marion Junction, 
100 yards from county line; new well; bored by a negro in 1902; depth, 143 
feet; water stands at -12 feet; stopped at first water. Record: Prairie 
soil; 0-15 feet; lime rock, 15-130 feet; sand rock, 130-131 feet; sand, 131-343 
feet. Broke tool in second sand rock at 143 feet. 



MARENGO COUNTY. 
Surface Features. 

The surface rocks in a narrow strip in the northern part of 
Marengo County are the upper members of the "rotten lime- 
stone," or Selma chalk. These rocks have the usual character, 
except that the limestone is at the top more mixed with clav 
than is generally the case and abounds in fossils, mainly 



WATERS OF THE CRETACEOUS. 183 

Uxogyra and Gryphaea. Next below the fossiliferous stratum 
comes a very purr whitish limestone, which is now utilized at 
Demopolis in the manufacture of Portland cement. This bed 
of pure limestone extends across the county by Van Dorn, 
Gallion, and Faunsdale to Uniontown and beyond. The strata 
of the Ripley formation outcrop in a belt just south of the 
Selma chalk. These beds are, in their disintegrated form at 
least, prevalently sandy, but below the zone of weathering they 
consist of sandy limestones or highly calcareous sandstones The 
sands which lie at the surface over all this Ripley belt might 
be supposed to indicate that this formation would be a good 
water bearer, but such is' not the case, at least so far as arte- 
sian waters are concerned, for in the Flatwoods belt adjoining 
the Ripley on the south, artesian borings have not generally 
resulted in overflowing wells. The surface sands give rise 
to fairly good w r ells, and springs are found along the edges of 
the ravines and washes', the water in both cases being usually 
rather strongly impregnated with lime. 

Although the Selma chalk outcrops only in the upper part of 
Marengo County, it is within this area that most of the artesian 
wells are found. These have a great thickness of the chalk to 
penetrate before reaching the water-bearing sands of the Eutaw 
and they are consequently deep. 

Artesian Records, 
demopolis and vicinity. 

At Demopolis, on Tombigbee River, artesian wells supply the town 
water works. The records of these borings are given below, together 
with those of other wells in and around the city. 

City well, Demopolis, in the S. E. quarter Section 24, Township tS. 
Range 2; bored by Jackson in 18S5; depth, 775 feet; flow, 50 gallons per 
minute. 

City, waterworks wells, Demopolis, in the S. E. quarter Section 24, 
Township IS, Range 2; No. 1, bored by Mr. Lipscomb in 1898; depth. 7-J5 
feet; diameter, 3 inches; water rises to 20 feet above the ground; origi- 
nal flow, 15 gallons per minute; present flow, 6 gallons per minute; tem- 
perature, 73°. No. 2, depth, 735 feet; diameter, 4 inches; water rises to 12 
feet above the surface; flow, 30 gallons per minute. 

New city wells, Demopolis, in the S. E. quarter Section 24, Township 18, 
Range 2; two wells, 50 feet apart; bored by J. I. Hawk in 1902; depth, 
900 feet; first flow at 800 feet; yield, about 150 gallons per minute. Record: 
Lime rock, 0-500 feet; sand, 500-900 feet; at about 700 feet in one well, a 
thin rock, very hard, not found in the other well. A sample of this water 
has been analyzed by Mr. Hodges, with the following results: 



] 84 DETAILS : COASTAL PLAIN DIVISION. 

Analysis of toater from wells of the Demopolis waterworks. 



Parts per million. 

Sodium (Na) 255.8 

Magnesium (Mg) 1.1 

Calcium (Ca) , 3.7 

Iron and alumina (Feo0 3 ,Alo0 3 ) 4.0 

Chlorine (CI) 40.6 

Sulphuric acid (SO*) trace 

Carbonic acid (HC0 3 ) 624.0 

Silica (Si0 2 ) 22.1 

951.3 



Leder Oil Company's well, Demopolis, on eastern edge of town, in the 
S. W. quarter Section 24, Township 18, Range 2; bored by Hawk in May, 
1902; depth, 765 feet; casing 325 feet, 4-inch and 2-inch; first water at 
550 feet, stand -10 feet; second water at 650 feet, stand -2 feet; third water 
at 750 feet, stand 10 feet above the ground; depth to principal supply, 750 
feet; original flow, 12 gallon per minute; depth to blue rock, 8 feet; 
thickness of blue rock, 500 feet. 

Demopolis Cooperage Company's wells, on eastern edge of town, in the 
S. W. quarter Section 24, Township 18, Range 2; bored in June, 1902, 
by Hawk, depth, 750 feet; casing 325 feet, 2 1-2-inch and 4-inch; first 
water at 525 feet, stand -2 feet; second water at 625 feet, stand 8 feet 
above the ground; third water at 735 feet, stand 20 feet above the ground; 
depth to principal supply, 735 feet; flow, 35 gallons per minute; depth to 
blue rock, 38 feet; thickness of blue rock, 485 feet. 

Demopolis Ice and Cold Storage Company's well, in the S. E. quarter 
Section 24, Township 18, Range 2; bored by Lipscomb in 1901; deptn, 835 
feet; casing, 300 feet, 4-inch, 535 feet 3-inch; first water at 525 leet; second 
water at 625 feet, flowing 6 gallons per minute; third water at 835 feet, 
flowing 60 gallons per minute; present flow (estimated), 35 gallons per 
minute. Record: Lime rock, 0-525 feet; sand, 525-575 feet; sand rock, 
575-576 feet; sand, with occasional thin rock, 576-835 feet. 

Well on George A. Kli place, Demopolis, in the S. E. quarter Section 
19, Township 18, Range 2; flows 1 1-2 gallons per minute; temperature, 
82°. 

John C. Webb's wells, Demopolis, in the S. W. quarter Section 24, 
Township 18, Range 2: No. 1, at Compress; bored by Stevens; estimated 
flow, 25 gallons per minute: temperature, 75°. No. 2, bored by Stevens; 
flow. 25 gallons per minute; temperature, 75°. 

John C. Webb's wells, near Demopolis: No. 1, on Sharp place, 3 1-2 
miles northeast of Demopolis; bored by Hawk in November, 1901; depth, 
661 feet; casing 350 feet, 2-inch and 4-inch; first water at 490 feet, stand 
-12 feet; second water at 550 feet, stand -4 feet; third water at 650 feet, 
stand 4 feet above the ground; depth to principal supply, 650 feet; original 
flow, 5 gallons per minute; depth to blue rock, 16 feet; thickness of blue 
rock, 430 feet. No. 2, on Baumgarten place, 4 miles southeast of Demop- 
olis; bored by Hawk in January, 1902; depth, 755 feet; casing 350 feet, 
2-inch and 4-inch; first water at 600 feet; -10 feet; second water 675 
feet, stand, -4 feet; third water at 750 feet, stand 8 feet above the ground; 
depth to principal supply, 750 feet; original flow, 10 gallons per minute; 
deptn to blue rock, 14 feet; thickness of blue rock, 540 feet. No. 3, on 
Sledge place, 4 3-4 miles south of Demopolis; bored by Hawk in July, 
1902; depth, 1040 feet; casing, 300 feet, 3-inch and 4-inch; first water at 



WATERS <>K THE CRETACEOUS. 1S5 

825 feet, stand —80 feet; second water at 950 feet, stand -70 feet; depth to 
principal supply, 950 feet; does not flow; pump used; depth to blue rock, 
It) feet; thickness of blue rook. 750 feet. 

Jesse Whitfield's wells, on Gaineswood place: No. 1, one-quarter mile 
south of Demopolis, in the N. 10. quarter Section 25, Township 18, Range 
2; flow decreasing so that it forms a kind of spring. .40. 2, 1 mile south 
of i>o. 1. in the N. E. quarter Section 30, Township is. Range 2; old well; 
no longer flows 

Gaineswood well, near Demopolis, one-halt' mile south of ice factory; 
in the N. E. quarter Section 25. Township 18, Range 2; bored about 1864; 
when the ice-factory well was bored this well ceased to flow. 

Alabama Portland Cement Company's well, at Spocari, near Demopolis, 
in the S. E. quarter Section 19, Township 18, Range 3; bored by Ste- 
vens in 1900; depth, about 750 feet; flow, 100 gaoons per minute; water 
rose to 20 feet above the ground; first water, at 475 feet, barely over- 
flowed; principal supply trom 750 feet. Record: Lime rock. 0-450 feet; 
sanu and thin sand rock, 450-750 eet: 

R. P. Knox's well. Demopolis; bored by Hawk in 1904; depth, 911 feet; 
flows. 

Bessie Minge Manufacturing Company's well, Demopolis, in Section 20, 
Township IS, Range 2; bored by Fred Braswell; depth, over 700 feet; 
400 feet through the lime rock; flow, 20 gallons per minute; temperature, 
75°. 

Black Warrior Lumber Company's well, Demopolis; bored by Hawk 
in 1904; depth. 700 feet; flows. 

_.. P. Allen's well. 3 miles south of Demopolis, N. E. quarter S. W. 
quarter Section 1. Township 17. Range, 2; bored by Stephens in 1895; 
depth, 1175 feet; casing. 1030 feet, 2-inch; estimated flow, 8 gallons per 
minute; water rises to 9 feet above the ground; overflow at 1030 and 1175 
feet. Record: Lime rock, 0-050 feet; sand with occasional rock, 050-1030 
feet; gravel, 1030-1040 feet; pink soapstone, 1040-1175 feet. 

D. H. Britton's well, in the N. half S. W. quarter Section 20, Township 
17, Range 4; old well; no record available. 

Well at Van Dorn station. 3 or 4 miles east of Demopolis; flows good 
stream. 

GALLIOX AXD VICINITY. 

Wells on Windsor place, owned by Thornton Tayloe, 2 miles south- 
east of Gallion, in the S. ualf Section 9, Township 17, Range 4, E.; four 
old wells: No. 1, flow, 2 gallons per minute; temperature, 74°. The four 
wells are in a radius of 1 mile; two of them no longer flow, and the 
fourth wen flows about 2 gallons per minute. 

Wen on Ross place, 6 miles south of Gallion, in the S. W. quarter Sec- 
tion 34, Township 17, Range 4, E. ; flow, one-half gallon per minute; 
water rises to 3 feet above the ground., temperature, 09°. 

FAUNSDALE AXD VICINITY. 

John Minge's well, on Body place. 5 miles southwest of Faunsdale; 
bored in 1903 by A. J. Dallings; no record since completion; first water, 
at 420 feet, stood at -6 feet. Record: Soil, 0-12 feet; blue rock, 12-420 feet; 
sand, 420-500 feet. 



186 details: coastal plain division. 

Well on Palmetto place, 3 or 4 miles southwest of Faunsdale; owned by 
Alex Archer; estimated flow, 4 gallons per minute; water rises to 4 
feet above the ground; temperature, 74°. 

Wells on Smaw place, 3 1-2 miles north of west of Faunsdale; three 
old wells; all flow from one-quarter to 1 gallon per minute; temperature, 
69°. 

Well on Gholson place, 2 1-2 miles north of west of Faunsdale; depth, 
300-500 feet; flows half-inch stream. 

Minge Wilkins's wells (old), 2 miles north of west of Faunsdale; bored 
about 1845: No. 1, depth, 360 feet; diameter, 3-inches; flow one-tenth 
of a gallon per minute. No. 2, three-fourths mile west of No. 1; depth, 
400 feet; flow, one-tenth of a gallon per minute. 

Wells on Selden place, 1 1-2 miles north of Faunsdale; two old bored 
wells, not flowing at present. 

C. D. Walker's wells, one-half mile northeast of Faunsdale; three oil 
wells, one of them barely flowing at surface, the other two having 
stopped; depth supposed to be about 450 feet. 

Mims Walker's wells, Faunsdale; five wells; depths, 450, 450, 560, 650. 
and 830 feet; start in the Selma chalk and obtain water from the Eutaw 
sands; four of them overflow with small streams; yield of one is 15 to 
20 gallons per minute; others can not be exhausted by deep-well pump; 
from the 830-foot well a windmill fills a 5,000- gallon tank in 12 hours 
with no decrease in volume. 

Well about 3 1-2 miles north of Faunsdale, reported to be 700 feet deep; 
yield, 8 gallons per minute; water rises to 2 1-2 feet above the ground; 
blue rock at a depth of 230 feet. 

Faunsdale Oil Mill well, bored by A. J. Dallings in 1901; depth, 700 
feet; diameter, 6 inches; water stands at -45 feet; air-lift used; level 
varies with amount pumped. Record: Blue rock, 0-400 feet; sand, 400-55(1 
feet; flint rock, 550-551 feet; sand, 551-625 feet; hard rock, 625-626 feet; sand, 
626-700 feet. 

J. C. Brown's well, Faunsdale; bored by a negro in 1899; depth, 560 
feet; first water at 540 feet, stand -70 feet, level lowered by pumping; 
second water at 550 feet, stands at -84 feet. Record: Marl, 0-540 feet; 
at 540 feet a thin stratum of sand, then 18 inches of flint rock, and 
greensand at bottom of boring. 

WEAK OLD SPRING HILL. 

Mrs. Charles Allen's well, 2 1-2 miles east of Old Spring Hill; depth, 
1400 feet; at 900 feet water stood at -30 feet; at 1400 feet water stood at -12 
feet. 



About Dayton are several wells which date from ante-bellum 
days and of which no records are now obtainable; but they 
have, according to the best available information, all gone 
through the limestone into the underlying Eutaw sands. 



WATERS OF TIIK CRETACEOUS. 187 



At Linden, which is on the extreme southern border of the 
Cretaceous, a well has been put down through the whole 
thickness of the Ripley formation and the "rotten limestone." 
As Linden is located near the lowlands of the Chickasabogue, 
the full thickness of the Ripley sands is not here present, as 
the record of the well will show. The well is in the court- 
house yard, and the record of the borings, as furnished by Prof. 
L. G. Biggers, is as follows : 

Record of Court House well, Linden. 



Feet. 

Clay 0—7 

Soft Limestone T--34 

Quicksand 34—58 

Blue sand 58—68 

Quicksand with mica 68-118 

Pure white sand 118—168 

Blue sand 16S--188 

Hard bluestone 188—190 

Soft shale or clay 193—322 

Light-colored limestone, like that at Demopolis. .322— 501 
Limestone, slaty and darker than the preceding 501—901 
Similar rock, but harder and ending below in a 

hard crust 901-1041 



At 1040 feet, a hard shell of stone was pierced, below which 
came a fine-grained, water-bearing sand. Below this, at 11 15 
feet, a limestone (or clay), very hard, to bottom of well; but 
the boring went down to 1200 feet, through soft limestone ( ?) 
and white and gray clay ; there was also some quicksand below 
the bed rock at 1 1 15 feet. The stream rises about 18 inches 
above the surface of the court-house yard, but the flow is very 
weak, only about 18 or 20 gallons to the hour ; temperature of 
the water is 73°, and the taste saline. It is said that a pump 
throwing 1 1-2-inch stream and worked continuously for seven 
or eight hours did not lower the water in the pipe below 16 
feet. If this is the case, the obvious means of increasing the 
flow would be to pipe off the water at this depth, and there is 
enough slope to accomplish this without trouble.* 



*Since the above was written this has been done, and a good flew 
is obtained at the present month of the well, 20 feet, more or less, be- 
low the level of the court-house yard. 



188 DETAILS : COASTAL PLAIN DIVISION. 

The Linden well and that at Livingston, Sumter County, are 
similarly located as' to geologic formations ; both pierce the 
Ripley and the whole thickness of the Selma chalk, though this 
is not quite so evident here as at Livingston. In both places 
the stream is weak and the water saline. 

The writer's interpretation of the record above is that the 
line between the Ripley and the Selma Chalk will fall some- 
where within the soft shale or clay, 132 feet thick, between 190 
and 322 feet ; and that the strata below that to 1 1 1 5 feet are 
the chalk formation, and the rest Eutaw, though, as' has been 
said above, this is not very apparent. 

The character of the water from the Linden public well is 
shown by the accompanying analysis by Mr. Hodges : 

Aanalysis of ivater from court-house well, Linden. 



Parts per million. 

Potassium (K) trace 

Sodium (Na) " 550.0 

Magnesium (Mg) 1.6 

Calcium (Ca) 7.2 

Iron and Alumina (Fe.,0 3 .Al 2 3 ) 5.0 

Chlorine (CI) 445.1 

Sulphuric acid (S0 4 ) trace 

Carbonic acid (HC0 3 ) 719.2 

Silica. (Si0 2 ) 17. S 

1745.9 



Southern Cotton Company well, Linden, in the S. B. quarter N. E. 
quarter Section 5, Township 15, Range 3; bored by S. W. Ingram in 1902; 
depth, 550 feet; casing, 80 feet, 6-inch; first water at 500 feet; second water, 
at 550 feet, stood at -18 feet; yield, 25 gallons per minute for a week, 
lowering level to -33 feet. 

Judge S. P. Pro well's well at Linden, about 200 yards north 
of depot. Depth 1100 feet; diameter 6 inches; casing to bot- 
tom. Present flow about one half gallon per minute at 6 feet 
elevation above the surface ; original flow 2 gallons per minute. 
Taste and effect decidedly those of epsom s'alts. Record, sand 
about 100 feet, then lime rock to depth not given. 

FLAT WOODS OR POST OAKS. 

South of Linden is the belt of Flatwoods or Post Oaks, as 
the lands have been called. The surface of this belt is occu- 
pied by the clays of the lowermost Tertiary. Near their contact 



WATERS OF Till-: CRETACEOUS. 189 

with the Ripley the clays are strongly limed by the washings 
from that formation and make a sort of black prairie country of 
great fertility. The main body of the Flatwoods, however, 
away from this contact, contains comparatively little lime. 
The surface is a trough between the sandy calcareous hills of 
the Ripley, on the one side, and the high Tertiary hills capped 
with the red loam and pebbles of the Lafayette, on the other. 
( )n account of the dearth of water during the summer and the 
excess of it during the winter, and spring, cultivation of the 
Flatwods land is out of the question, except locally where a 
remnant of sand of an overlying formation has escaped removal 
by denudation. For water the few inhabitants, mostly negroes, 
depend on cisterns dug into the clay and filled from the house- 
tops. Another drawback to cultivation of the Flatwoods is 
the defective drainage, but this might be overcome if the water 
problem were solved. 

The following notes concerning the artesian borings in the 
Flatwoods of Marengo County have been furnished by Mr. 
C. B. Wooten, of Consul. These examples will serve to show 
that good water may be obtained in the Flatwoods by deep 
borings. 

In the vicinity oi Whitehall, 15 miles east of Linden, in 185;' 
and 1858, seven wells were bored in or near the plantation of 
Colonel Watts, in the midst of the Flatwoods or Post Oak belt. 
These wells ranged in depth from 350 to 800 feet; the first 
water struck in any of the borings was at 320 feet, and it rose 
to within 40 or 50 feet of the surface ; water was sulphurous 
and chalybeate. Colonel Watt's place was 2 miles south of the 
Linden and Cahaba road, 6 miles from McKinley, and 2 miles 
from Thomaston. 

Mr. W'ooten, in 1858, had a well bored to the depth of 320 
feet, getting splendid water which rose to within 60 feet of 
the surface. 

Since the completion of the Louisville and Nashville railroad 
to Myrtlewood. several deep wells have been sunk within the 
territory of the Flatwoods. These borings, however, do not 
seem to have obtained any water from the Ripley s'ands, but 
have gone through the Selma chalk into the Eutaw sands, like 
the well at Linden. Through the courtesy of Mr. J. R. Nevers 
we are enabled to give some account of a deep well at Cates. 
in Section 10, Township 15, Range 2 east. 



190 details: coastal plain division. 

Well at Cates: Depth 1140 feet; diameter 3 inches; cased with 3-inch 
casing to depth not given; depth to water 1120 feet; overflowing 25 gal- 
lons per minute. No decrease since the beginning in 1906. The water is 
salty and is used only for drinking purposes. It is said to be of about 
the same character as the water from the Livingston well in Greene 
county. 

Record: Clay 0- 12 feet; black soapstone (Sucarnochee clay) with a 
little sand but no water, 12- 162 feet; limestone (Selma chalk) with occa- 
sional hard ledges, 162 - 1000 feet; hard rock, 1000 - 1080 feet; water bearing 
sands, 1080 - 1140 feet. No water was obtained until the depth of 1080 feet 
had been reached; the water bearing sands are 60 feet in thickness and 
the strainer of the well rests on the next rock below the sands. The well 
yields a good deal of gas at all times. The water rises to an elevation of 
40 feet above the surafce. 

LOWER PAST OF THE COUNTY. 

The lower part of Marengo County is underlain by sands and 
clays of the Tertiary formations, which in most places still 
have the capping- of the red loam and pebbles of the Lafayette. 
Surface waters are therefore generally ample in quantity and 
excellent in quality, so that artesian borings are hardly needed. 
In these sections, however, where clays predominate in the sur- 
face outcrops, it would in many cases be much to the advantage 
of the citizens to get better water than can be had from shallow 
wells and springs. In such places there should be no trouble 
in obtaining artesian water, as is shown by the boring at Butler, 
Choctaw County, where the strata are similar to those in Ma- 
rengo County. 



DALLAS COUNTY. 
General Conditions. 

Within the limits' of Dallas County all four divisions of the 
Cretaceous outcrop are at the surface and determine the soils, 
the topography, and the water conditions. The two lower di- 
visions (Tuscaloosa and Eutaw) appear only in a narrow strip 
in the northeast corner of the county, between Oakmulgee and 
Mulberry creeks, in Townships 18 and 19. In the greater par!: 
of this section the red loam and pebble beds of the Lafayette 
oyerlie the strata of the older formations and determine the 
s'oils and water conditions. Surface wells and springs yielding 
the best freestone water are not lacking in this section, and while 



WATERS OF THE CRllTACEOUS. 191 

no artesian wells are recorded there be no difficulty in getting 
artesian water within reasonable depths from cither the Tus- 
caloosa or Entaw sands. 

North of Alabama River, about the city of Selma,, is a wide 
terrace, 75 to 1 00 feet above river level, on which the red loam 
and pebbles of the Lafayette formation overlie the calcareous 
beds of the Selma chalk. The immediate surface about Selma 
and for a number of miles' up and down the river is formed by 
sands, probably of a later formation than the Lafayette (Colum- 
bia or Ozark sands). Beyond this terrace the chalk forms the 
surface, as a rule, to the north, west, and southwest of Selma. 

In all this section down to a northwest-southeast line run- 
ning approximately parallel to Chilatchee creek and 3 miles 
distant from it, water must necessarily come from artesian bor- 
ings, except where the Lafayette and Columbia sands overlie 
the chalk and afford the usual abundance of freestone water 
from wells and springs. 

In crossing the county from Rehobeth, Wilcox County, by 
way of Crumptonia, Orrville, and Marion Junction, one sees 
very little of the chalky limestone except near the crossing of 
Boguechitto Creek, the surface being formed mainly by the La- 
fayette and Columbia sands and loams. Near Marion Junc- 
tion the chalk begins. The reason for this seems to be that this 
road follows generally the lowlands of Boguechitto Creek and 
its tributaries, where erosion has been more than usually ef- 
fective. The sands and loams of this mantle appear to be of 
the same nature as the terrace sands near Selma. Not many ar- 
tesian wells are found along this road, but the surface wells 
seem to afford sufficient water to meet the demand. From 3 
or 4 miles south of Marion Junction to the northern and west- 
ern boundaries of the county, the chalk occupies the surface. 
At Marion Junction ( altitude ( 204 feet) the wells do not over- 
flow, and windmills are used for raising the water. The depth 
of wells here is reported to be only 250 feet. 

A belt 8 or 10 miles wide in the lower part of Dallas Coun- 
ty, is underlain by the strata of the Ripley formation, in which, 
so far as the writer's information goes, no bored wells have 
been sunk. Much of the surface, however, throughout this 
belt is formed by the Lafayette sands and loams, in which sur- 
face wells afford a sufficient supply of water. 



192 details: coastal plain division. 

East of Alabama River the conditions are about the same as 
those above described for the area underlain by the chalk and 
the Ripley. The divides in this part of the county, in the ter- 
ritory of both these formations, are often high, level plains, with 
a surface of red loam underlain by pebbles (Lafayette). Rich- 
mond, Carlowville, and Pleasant Hill are upon such high pla- 
teaus. The lowlands have strong calcareous soils (Selma chalk 
and Ripley), entirely different from the sandy loams of the pla- 
teaus. 



Artesian Records. 



The details below of the bored wells of Dallas County, will 
illustrate its artesian conditions. 



The old town of Cahaba was probably one of the first places 
where artesian borings were made in Dallas' County. One of 
these, "the great well," is said to yield 1200 gallons of water per 
minute, which if true, would make it probably the largest in 
the State except the Roberts well in Escambia County. The 
great well on the Pickens place, in Hale County, yields now- 
only about 850 gallons per minute, and it, also, has the reputa- 
tion of being the largest in the State. It is probable that the 
flow in both these wells has' much diminished since they were 
first bored, by reason of leakage and the stopping or partial 
stopping of the pipe by stones and other obstructions. The rec- 
ord of the Cahaba well, as published by Professor Winchell.* 
(furnished to him by Mr. Campbell, who bored it), is as fol- 
lows : 



*Proc. Am. Assoc. Adv. Sc. 185G, section on Geolcgy, p. y9. 



WATERS Or" THE CRETACEOUS. 193 

Record of the "great well,'' Cahaoa. 



Feet. Inches. 

Loam, red clay, sand, and pebbles ;!2 10 

First "rotten limestone" 330 10 

First sandstone (a concrete of sand and shells) 6 

Gray sand, with water 3 

Second sandstone 1 3 

Gray -sand 2 5 

Sticky sand and clay 2 9 

Sand and "rotten limestone" (?) (clay) 7 9 

Sticky sand and clay 19 9 

Greensand 1 6 

Gray sand, with water 129 10 

Third sandstone 11 

Gray sand, with water and streaks of "rotten lime- 
stone 51 — 

Bluish sand, with two streaks of reddish sand 32 — 

Bluish-gray and laminated clay 27 6 

Dark-gray sand, with water 26 — 

Bluish-gray sand and clay, with water 59 8 

736 6 



The interpretation which might be given to this' record is 
Hypothetical record of "great well" Cahaoa. 



Feet. 

Sands, loams, and pebbles of the Lafavette 32.83 

Selma chalk 380.83 

Eutaw sands 227.66 

Tuscaloosa sands and clays 145.16 

740.59 



This might possibly serve to indicate that borings into the 
Tuscaloosa formation in other places would yield a greater 
flow of water than those that go merely into the Eutaw sands. 
The general impression among the well borers is that when they 
reach the pink kaolin or soapstone, as it is often called, no in- 
crease in the supply will be obtained for at least ioo or 200 feet. 
Allowance must, of course, always be made for variations In 
the thickness of the beds of massive clay occurring in the Tus- 
caloosa formation, since they are sometimes 200 feet or more 
thick. It would probably be worth while in many cases to con- 
tinue the borings through these clays when a sufficient supply 
of water has not been found above them. 

From Dr. Winchell's paper above cited some additional rec- 
ords are taken of the old artesian wells about Selma and Ca- 
haba, before details of the more recent borings are given. Re- 

13 



194 



DETAILS I COASTAL PLAIN DIVISION. 



sides the "great well," he mentions the court-house well (depth, 
555 feet; temperature, 75°), and the well at Bell's Hotel (depth, 
40.0 feet; temperature, 74°), both in the town of Cahaba, where 
there are at least 15 old wells flowing 10 to 30 gallons per min- 
ute and varying in temperature from 74° to 76°. Dr. Winched 
also records a well on the opposite side of the river, near Ca- 
haba, on the plantation of E. P. Watts, bored by Crow & Read 
(depth, 275 feet; flow, 20 gallons per minute) ; and two wells 
on the plantation of Freeman King, 5 miles below Cahaba, also 
on the opposite side of the river, each 560 feet deep and yield- 
ing 250 gallons per minute. 



Selma and Vicinity. 
Dr. Winched gives records' of 11 wells in Selma, as follows: 
Record of wells in Selma. 



Location. 



Depth. 



Yield. 



Borer. 



Feet. 



Junction of Main and Water Sts. 

Main street, north of No. 1 

Main street, north of No. 2 

Residence of Abner Jones 

Residence of J. Lapsley 

Foundry 

Machine shop ...* 

Mr Hall's 

Russell & Berry brickyard 

Harrison's brickyard , . 

Blevins & Edwards's 



Gallons 

per 

minute. 

470 jMr. Crow. 

380 100 | Mr. Crow. 

334 40 Mr. Crow. 

12 Mr. Crow. 

330 25 | Mr. Crow. 

230 [Mr. Campbell. 
360 300(?)IMr. Crow. 

340 100 I Mr. Crow. 

350 300 I Mr. Crow. 

360 300 | Mr. Crow. 

.Not given | Not given | 



Cawthon Cotton Mills well, Selma; bored in 1899 by J. I. Hawk; flows? 
115 gallons per minute; depth to blue rock, 30 feet; thickness of blue rock, 
250 feet; well starts in "rotten limestone" and water supply is from Butaw 
sands. 

City waterworks wells, Selma: six wells ranging in depth from 425 to 
500 feet, all of whi.ch overflow or are pumped into reservoir; bored in 
1888; temperature, 63°. Four 5-inch and 6-inch wells, with depths of 
from 500 to 700 feet, are located at main station; water rises 3 feet above 
the surface, but is pumped for distribution by the air-lift process; total 
flow from four wells, 38,000 gallons per hour. The following analysis by 
Mr. Hodges shows the composition of the water of the city supply at 
Selma: * 



WATERS <U' THE CRETACEOUS. 195 

Analysis of water from city waterworks wells, Seh»a. 

Parts per million. 

Potassium ( K ) 5.4 

Sodium (Na) 12.0 

Magnesium (Mg-) 2.3 

Calcium (Ca) 19.3 

Iron and alumina (I-V,<> : . Al 2 O s 1.0 

Chlorine (CI) 6.8 

Sulphuric acid (SO,) 9.6 

Carl. <mir acid (HCO :i ) 86.5 

Silica (SiO a ) 33.0 

175.9 



City waterworks well, No. 4, Selma; bored by John Bicksler in 1903; 

cased to bottom with 6-inch, 8-inch and 11-inch casing depth, 655 feet; 

estimated flow, 300 gallons per minute; boring stopped in fourth water. 

Record of city waterworks well No. 4, Selma. 

Feet. 

Clay — 14 

Sand and gravel 14 — 18 

Blue rock 18— 34 

Hard rock 34 — 35 

Blue rock 35 — 165 

Greensand 165 — 180 

Hard rock 180 — 182 

Sand and water (rising to —9 feet) 182 — 272 

Marl 272 — 290 

Sand and gravel 290 — 302 

Red marl 302 — 310 

Soapstone 310 — 427 

' Hard rock 427 — 532 

Red Marl 532 — 572 

Sand and gravel 572 — 655 



Well at the council chamber, Selma; depth, 620 feet; gives good flow; 
starts in the "rotten limestone" and obtains water from the Tuscaloosa; 
altitude, 121 feet; temperature, 62°. 

C. C. Ferrill's well, 1 mile from court-house, Selma; bored in 18S4 
by Peyton Hatch; depth, 487 feet; flow, 110 gallons per minute; tempe- 
rature, 68°; starts in the "rotten limestone" and obtains water from 
the Eutaw sands or Tuscaloosa formation; depth to blue rock, 125 feet; 
altitude, 121 feet. 

Analysis of water from C. C. Ferrill's well, Selma. 
{Analyst, R. ' S. Hodges.) 

Parts per million. 

Potassium (K) 6.5 

Sodium (Na) 6.9 

Magnesium (Mg) l.S 

Calcium (Ca ) 21.3 

Iron and alumina (Fe<,0 3 . Al,0 :i ) 1.8 

Chlorine (CD 3.4 

Sulphuric acid (S0 4 ) ■-. 6.4 

Carbonic acid (HCO a ) S8.2 

Silica (Si0 2 ) 18.6 

154.9 



196 DETAILS: COASTAL PL AI1S DIVISION. 

E. Gilman's well, Selma; bored in 1899 by J. I. Hawk; depth, 643 feet; 
flows 85 gallons per minute; 4-inch casing to blue rock, balance 2 1-2-inch; 
water carries some iron; altitude, 121 feet. 

Record of E. Gilman's well, Selma. 



Soil 0— 28 

Blue rock 28 — 90 

Sand and sand rock 90 — 100 

Sand, sandrock, and layers of soapstone 100 — 480 

White clay 480 — 520 

Pink kaolin 520 — 600 

Sand, gravel, some red clay 600 — 643 



H. A. Harralson's well, Selma; bored in 1875; depth, 780 feet; diameter, 

4 inches; flow small and charged with iron; starts in "rotten limestone" 
and obtains water from the Tuscaloosa formation. 

Hestell Cotton Mill well, Selma; bored by Patrick Oilman; depth, 465 
feet; yield, 80 gallons per minute; starts in "rotten limestone" and ob- 
tains water from Butaw sands and Tuscaloosa formation; altitude, 121 
feet. 

McGill well, corner of Broad street, near union depot, Selma; flows 12 
gallons per minute from 2-inch pipe; temperature, 68°; altitude, 121 feet. 

Well at People's Oil Mills, Selma; bored in 1900; started in the "rotten 
limestone" and obtained water in Tuscaloosa beds; altitude, 121 feet. 
Record unknown. 

Race track well, Selma; stated to be 3 inches in diameter and to yield 
150 gallons per minute; temperature, 68°; water charged with iron; starts 
in "rotten limestone" and obtains water from the Butaw sands or Tus- 
caloosa beds. 

J. L. Schweizer's well, at residence, two blocks northwest of Southern 
Railway passenger depot, Selma; bored by Hawk in December, 1900; 
depth, 450 feet, casing, 400 feet; 2 1-2-inch and 4-inch; first water at 100 
feet, stand — 10 feet; second water at 210 feet, stand — 2 feet; third water 
at 320 feet, stand 3 feet above the surface; fourth water at 450 feet, stand 

5 feet above the surface; depth to principal supply, 450 feet; flow, 20 
gallons per minute; depth to blue rock, 30 feet; thickness of blue rock, 
65 feet. 

J. M. Baker's well, at residence, 1410 Selma street, Selma; bored by 
Haw-.c in February, 1901; depth, 665 feet; casing, 2-inch, 3-inch and 4-incii; 
first water at 100 feet, stand —20 feet; second water at 210 feet, stand 
—12 feet; third water at 320 feet, stand —7 feet; fourth water at 465 feet,- 
stand —2 feet; depth to principal water supply, 6&0 feet; flow, 150 gallons 
per minute; depth to blue rock, 35 feet; thickness of blue rock, 65 feet. 

Knox Academy well, corner of North and Mabry streets, Selma; bored 
by Hawk in November, 1902; depth, 615 feet; casing, 615 feet, 2 1-2-inch 
and 4-inch; first water at 100 feet, stand —20 feet; second water at 210 
feet, stand —12 feet; third water at 325 feet, stand —4 feet; fourth water 
at 450 ieet, stand —4 feet; depth to principal water supply, 610 feet; 
original flow, 96 gallons per minute; depth to blue rock, 31 feet; thickness 
of blue rock, 75 feet. 

There are perhaps as many as ioo smaller wells in the city 
of Selma in which the water stands near the surface and is 



GEOLOGICAL SURVEY OF ALABAMA. UNDERGROUND WATER RESOURCES. PLATE XVI. 




A. Well in -Elkdale Park, Selma, Dallas County. 




>w 






•• 



B. Old Road Showing Grand Gulf Strata Capped with Lafayette near 
Gaikestown Ferry, Clarke County. 



WATERS OF THE CRETACEOUS. 197 

raised by pumps ; but no reliable records could be obtained of 
these. 

Buckley Cotton Oil Axil! well, Selma; bored by John Bicksler in L892; 
depth, 500 feet; first water, at 09 feet, stood at — 8 feet; second water, at 
170 feet, stood at surface; third water, at ISO feet, overflowed; fourth 
water, at 500 feet; overflowed; yield, 300 gallons per minute. 

Record of Buckley Cotton Oil Mill well, Selma. 



— 


20 


20 — 


28 


28 — 


32 


32 


34 


34 — 


38 


38 — 


41 


41 — 


67 


67 — 


69 


69 — 


88 



Feet. 

Sand 

Gravel 

Soapstone 

Shell 

Sand 

Lime rock 

Sand 

Hard rock 

Sand and water (rising to — 8) 

Soapstone 88 — 98 

Soft sandstone 98 — 170 

Sand and gravel (overflow) 170 — 173 

Hard rock 173 — 176 

Coal 176 — 177 

Sandstone 177 — 180 

Marl 180 — 186 

Sand (overflow) 186 — 190 

Soapstone 190 — 196 

Sandstone 196 — 230 

Red sand 230 — 242 

Sand 242 — 280 

Rock 280 — 288 

Sand and gravel (water increasing) 288 — 500 



Well at Elkdale Park, Selma, (Plate XVI. A.) in the N. E. quarter Sec- 
tion 24, Township 17, Range 10; bored by John Bicksler in 1902; depth 656 
feet; first water at 165 feet, stood at —7 feet; second water, at 375 feet, 
overflowed; third water, at 600 feet, flows 300 gallons per minute; tem- 
perature, 72°. Mr. Bicksler thinks that the flow has increased to 400 gal- 
lons in two years. 

Record of well at Elkdale Park, Selma. 



Feet. 

Clay 0— IS 

(?) 18— 34 

Soapstone 34 — 55 

Greensand 55 — 83 

Blue rock 83 — 165 

Sand (water rising to — 7 feet) 165 — 170 

Soapstone 170 — 195 

Blue marl 195 — 202 

Marl 202 — 375 

Gravel and sand (overflow) 375 — 384 

Rock 384 — 386 

Sand 3S6 — 395 

Red marl 395 — 420 

(?) 420 — 600 

Sand and water 600 — 656 



198 DETAILS : COASTAL PLAIN DIVISION. 

Andrew Gill, of Selma, is authority for the following: On 
his place two blocks west of the ice factory, is' a well bored in 
1885, which ordinarily flowed 10 to 15 gallons per minute, but 
when the ice-factory well was bored the flow was weakened. A 
pump is used in the ice-factory well and when this is in opera- 
tion the Gill well ceases flowing entirely. The same is true of 
two other wells in the vicinity, one owned by Mr. Schweizer 
and another by Eugene Robbins. Mr. Schweizer's well is 4 
years old, Robbin's well 18 years, and the ice-factory well 18 
years. Several years ago Proctor & Gamble bored a well at the 
cotton-oil mill. At about 450 feet they got an overflow which 
caused the three wells mentioned above to stop, also C. C. Fer- 
rill's well, 250 yards southwest of the oil mill, and a well at the 
Hestell Cotton Mills, one-quarter of a mile west of the oil-mill 
well. The wells all stopped entirely until Proctor & Gamble 
cased against the 450-foot water, when they began to flow 
again. When Colonel Abbott had the Elkdale Park well bored, 
in 1902. several wells' in the vicinity were shut off and the> 
have never flowed since that time. 

Well at Summerfield Oil Mills, Selma; bored in 1899; depth, 465 feet; 
diameter, 6 inches; flow, 100 gallons per minute; cased to blue rock; 
starts in "rotten limestone" and obtains water from the Butaw sands 
or from the Tuscaloosa formation; altitude, 121 feet. 

Well on Welch plantation, 3 miles northwest of Selma; bored in 1899 
by J. I. Hawk; flow, 18 gallons per minute; depth, 424 feet. Blue rock from 
18 to 138 feet, balance sand and soapstone. 

Well at Durands Bend, about 6 miles northwest of Benton; in a dilapi- 
dated coiidition and forms a kind of spring; flow was probably 10 or 
15 gallons per minute; tempe'rature, 70°. 

Andrew Gill's well, 7 miles west of Selma; bored in 1899 to a depth of 
365 feet; yield by natural flow, 30 gallons per minute; starts in "rotten 
limestone" and obtains water from the Eutaw sands. 

W r ell owned by Mrs. L. R. Jones, of Selma, 3 miles southwest of Selrna, 
in the N. W. Quarter N. E. quarter Section 34, Township 17, Range 10; 
estimated flow. 30 gallons per minute. 

Well owned by Mrs. Carroll, of Montevallo, 3 miles west of Selma, in 
the S. W. quarter S. W. quarter Section 26, Township 17, Range 10; flow, 
2 gallons per minute; reported to have had much stronger flow until a 
well was bored one-half mile east. 

Wells on Hunter place: No: 1, 5 miles southwest of Selma, in the N. W. 
quarter N. E. quarter Section 8, Township 16, Range 10; 200 yards east 
of the Southern Railway; flow, 5 gallons per minute; temperature, 68°. 
No: 2, 1 mile north of No. 1, in the N. W. quarter Section 4, Township 
16; Range 10; flow, 5 gallons per minute; temperature, 68°. 

Well on Sanders place, 4 1-2 miles north of Cahaba, 5 miles southwest. 
of Selma, in the N. E. quarter S. W. quarter Section 8. Township 16, 
Range 10; flow, 2 gallons per minute; water rises 1 foot above the ground; 
temperature, 70°. 



WATERS OF Tin; CRETACEOUS. 199 

ALONG THE LOTJISVSLLE AM) NASHVILLE RAILROAD. 

Well at crossing of Cahaba River; depth, 590 feet; diameter, 6 inches, 
water rises :':' feet above the surface; yield, 80 gallons per minute; 
temperature, 70°: reported in 1899. 

W'.ll at. Salt Marsh ("Sugar Bottom"), 1 mile east of Beloit, on South- 
ern Railway, in fraction B, N. E. quarter Section 14. Township 1(5, 
Range 9; Hew. 20 gallons per minute; water rises 5 feet above the ground; 
temperature. ._'. 

Two other wells are recorded on the line of this railroad, but without 
sufficient notes of exact locality: No. 1. depth, 4S7 feet; diameter, (i 
inches; water rises 28 feet above the surface; flow, 110 gallons per minute; 
temperature, G8°. No. 2, depth, 600 feet; diameter, 6 inches; flow, 80 
gallons per minute; water rTSes 16 feet above the ground; temperature, 72' J . 



ORRVIIXE AND VICINITY. 

Town well. Orrville; bored by a negro in 1900; depth. 635 feet; water 
stands at —17 feet; first water at 404 feet; second water at 635 feet, stands 
at —17 feet. Record: Soil. 0-50 feet; blue rock, 50-401 feet; sand rock, 
with water- worn pebbles, 401-404 feet. Steam pump used and water was 
not lowered. 

Ellis & Dunaway's well, Orrville. 300 yards north of town well, in 
the N. W. quarter Section 2, Township 15, Range 8; bored by John Bicks- 
ler in 1902; depth, 1088 feet; first water at 545 feet; second water, at 730 
feet, rose 1 foot above the surface; third water not given; fourth water, 
at 1088 feet, stood at —11 feet. 100,000 gallons per day have been pumped 
from the well and the level not lowered. 

Well on J. P. Milhous place, 3 miles west of Orrville, on south side 
of Louisville and Nashville Railway, in the S. E. quarter Section 32, 
Township 16. Range 8; flow, 6 gallons per minute; water rises 2 feet above 
the surface; temperature, 73°. 

MARTIN'S STATION AND VICINITY, LOUISVILLE & NASHVILLE RAILROAD. 

Louisville and Nashville Railroad well, Martins Station, in the N. \V. 
quarter S. E. quarter Section 31, Township 16, Range 8; bored by Bicksler 
in 1900; depth, 755 feet; water rises 27 1-2 feet above surface, and keeps 
railroad tank full; temperature, 76 1-2°. 

A. J. Martin's wells: No. 1, three-fourths mile northwest of Martins 
Station, in Section 31, Township 16, Range 8; flow, 1 1-2 gallons per minute; 
water rises 3 feet above the surface; lemperature. 75°. No. 2, 1 mite 
west of Eleanor, in the N. W. quarter N. W. quarter Section 36. Township 
16, Range 7; flow, 1 gallon per minute; water ris s 3 feet above tne sur- 
face; temperature, 74°. 

Craig Smith's well, 4 1-2 miles west of Martins Station; old well, m 
decay. 

E. B. Martin's wells: No. 1, 1 1-2 miles southwest of Martins Station, 
in the S. E. quarter N. E. quarter Section 1, Township 15. Range 7: an 
old flowing well; flow, 5 gallons per minute; water rises 4 feet above the 
ground; temperature, 74°. No. 2, one-fourth mile southwest of Martins 
Station, in the S. E. quarter S. W. quarter Section 31, Township 16, Range 
8; very weak stream; pump used; temperature, 70°. 

Phil Milhous's old wells: No. 1, 3 miles southwest of Martins Station, 



200 details: coastal plain division. 

in the N. W. quarter N. E. quarter Sec. 2, Township' 15, Range 7; flow, 3 
gallons per minute; water rises 3 feet above the surface; temperature, 77°. 
No. 2, one-half mile northwest of No. 1, near center of Sec. 35, Township 
16, Range 7; flow, 3 gallons per minute; water rises 3 feet above the 
surface; temperature, 75°. No. 3, flows a very weak stream, no partic- 
ulars. 

Mrs. F. M. Hunter's well, 1 1-2 miles south of Martins Station, in 
Section 7, Township 15, Range 18; old flowing well; yield, 6 gallons per 
minute. 

Well on Wilson place (owned by A. J. Martin) 1 mile norm of Mar- 
tins Station, in the N. W. quarter S. E. quarter Section 30, Township 16, 
Range 8; flow, 3 1-2 gallons per minute; water rises 5 feet above the 
surface; temperature, 71 1-2°. 

Dr. J. P. Purniss's old well, 2 miles southwest of Martins Station, in 
the N. E. quarter Section 11, Township 15, Range 7; now, 5 gallons per 
minute. 

NEAR LINES OF SOUTHERN RAILWAY. 

Wells on Elijah Bell place: No. 1, 1 1-4 miles south of Brown's Station, 
in the S. E. quarter N. W. quarter Section 27, Township 17, Range 7; 
flow, one-eighth gallon per minute; water r ses 4 feet above surface; 
temperature, 69°. No. 2, one-half mile southeast of No. 1, in the N. W. 
quarter S. E. quarter Section 27, Township 1/, Range 7; flows; no record. 

A. C. Davidson's well, 1 mile west of Brows Station, in the N. ni. quar- 
ter N. W. quarter Section 21, Township 17, Lange 7; flow used for ooiler 
in sawmill; could not be measured. 

Well on Clark place, near Browns Station, in the N. W. quarter Section 
34, Township 17, Range 7: old well; flow, 3 gallons per minute; water 
rises 3 feet above the ground; temperature, 70 1-2°. 

Wells on Nelson place: No. 1, 2 miles southwest of Browns Station, 
in the N. E. quarter Section 29, Township 17, Range 7; flow, 2 gallons 
per minute; water rises 2 feet above the ground; temperature, 70°. No. 
2, one- fourth mile west of No. 1; flow, one-half gallon per minute; water 
rises 3 feet above the surface; temperature, 69°. No. 3, one-fourth mile 
west of No. 1: flow, one-half gallon per minute; water rises 4 feet above 
the surface; temperature, 69°. No. 4, one-fourth mile east of No. 1; flow, 
3 gallons per minute. 

Wells on Turner Bell place, 4 miles southeast of Browns Station: No. 
1, in the S. E. quarter S .W. quarter Section 2, Township 16, Range 7; 
flow, 1 gallon per minute; water rises 4 feet above ground; temperature, 
69° No. 2, in the S. W. quarter S. W. quarter Section 2, Township Hi. 
Range 7; flow, 1 gallon per minute; water rises 3 feet above the surface; 
temperature, 70°. 

The following wells near Brown's Station were inaccessible, and no 
records are available. On the Buck Bell place, in the S. E. quarter S. E. 
quarter Section 3, Township 16, Range 7; 

the Parnell place, in "the S. E. quarter N. E. quarter Section 35, Town- 
ship 17, Range 7; 
the Bland place, in the S. E. quarter Section 26, Township 17, Range 7: 
the A. C. Coats place, in the N. W. quarter Section 26, Township 17, 
Range 7. 

Kendrick Brothers' wells, Massilon: No. 1, at Massilon, in the S. E. 
quarter N. W. quarter Section 20, Township 17, Range 8; bored by Pey- 
ton Hatch; depth, 280 feet; casing, 45 feet, 4-inch; water stands at —36 
feet; windmill used; first water at 280 feet. No. 2, at Massilon, 'in the 



WATERS OF THE CRETACEOUS. 201 

S. E. quarter N. W. quarter Section 20, Township 17, Range 8; bored in 
1901 by Tom Reid; depth, 2S0 feet; casing, 35 feet, 4-inch; water stands at 
■ 15 feet; probably stopped on rock just above second water. No. ;'.. 
300 yards east of No. 1; old well; depth, 280(?) feet; water stands at — W'l 
feet. No. 4, 700 yards east of No. 1; old well; depth 280(?) feet; water 
stands at — 24 feet. No. 5, 1 1-4 miles east of No. 1, in the S. W. quarter 
N. E. quarter Section 21, Township 17, Range 8; bored by Tom Reid in 
1898; depth, 285 feet; water stands at —45 feet. r.o. t>, 2 1-2 miles southeast 
of No. 1, in the S. W. quarter Section 27, Township 17, Range 8; old 
flowing well; no record. No. 7, in the N. W. quarter N. W- quarter Sec- 
tion 20, Township 17. Range S; bored in 1901 by Tom Reid; depth, 280 feet; 
water stands at — 45 feet. No. 8, 1 1-2 miles northwest of No. 1; old flowing 
well; no record. No. 9, 1 3-± miles northwest from No. 1; old flowing well; 
no record. 

Wells on Jones estate, 1 1-2 miles southwest of Massilon; 4 old wells, 
now in decay; pumps used. 

W. H. Kendrick's wells, 3 miles southwest of Massilon: No. 1. in 
the S. E. quarter N. W. quarter Section 31, Township 17, Range 8, on 
top of hill; water stands at — 32 feet. No. 2, in the S. W. quarter N. W. 
quarter Section 31, Township 17, Range 8, at foot of hill, 100 yards north- 
west of No. 1 and 35 feet lower; flows very weak stream. No. 3, S. E. 
quarter N. W. quarter Section 31, Township 17, Range 8, 150 yards east 
of No. 1; water stands at —20 feet. 

Well on S. W. John's place, 1 mile west of Massilon, in the N. E. quarter 
N. W. quarter Section 19, Township 17, Range S; old well; flowing 5 gal- 
lons per minute; temperature, 74° 

C. O. Jones's well, near Massilon, in the S. W. quarter N. W. quarter 
Section 30, Township 17, Range 8; flow, 1 gallon per minute; water rises 
to 1 foot above the ground; temperature 70°. 

Wells on Mrs. King's place, near Massilon; No. 1. 1 1-4 miles west of 
Massilon, in the S. "W. quarter N. W. quarter Section 19, Township 17. 
Range S; flow, 1 1-2 gallons per minute; water rises o feet above surface; 
temperature, 72°. No. 2, 2 miles west of Massilon, in the N. W. quarter 
N. W. quarter Section 25, Township 17, Range 7; flow, 1 gallon per minute; 
water rises 3 feet above the ground; temperature, 69°. No. 3, three- 
fourths mile west of No. 1, in the S. W. quarter N. W. quarter Section 
30, Township 17, Range 8; flow, 1 gallon per minute; water rises 2 feet 
a^ove the surface; temperature, 69°. No. 4, at house, in the S. W. quarter 
S. W. quarter Section 19, Township 17, Range 8; flow, 1 gallon per minute; 
temperature, 69°. No. 5, at house, in the S. W. quarter N. W. quarter 
Section 19, Township 17, Range S; flow. 1 galon per minute. 

Mrs. E. W. Fort's well, 1 mile north of Marion Junction, in the N. E. 
quarter Section 14, Township 17, Range 8; depth, 900 feet; water stands 
at — o feet. 

Mitchell we.., owned by H. P. Randall, in the S. E. quarter S. E. quar- 
ter Section 22, Township 17, Range S; estimated flow, 2 gallons per minute; 
temperature, 71°. 

Well on Harrell p'lace, 2 1-2 miles southwest from Marion Junction; in 
the N. W. quarter Section 27, Township 17, Range 8; owned by Ken- 
drick Brothers, of Massilon; flow, 1-2 gallon per minute; temperature, 
68°. This well is located somewhat lower than the Mitchell well. 

Pegues well, 3 miles south of west of Marion Junction, in the S. E. 
quarter S. E. quarter Section 29, Township 17, Range 8; flow has de- 
creased and water stands at surface. 

Rascoe well, 3 1-2 miles southwest of Marion Junction, in Section -S 
Township 17, Range 8; owned by M. E. Smith, of Marion Junction: flow 
1 gallon per minute; water rises 2 feet above surface; temperature, 69°. 



202 details: coastal plain division. 

Well on Overstreet place, 4 miles southwest from Marion Junction, in 
Section 33, Township 17, Range 8; old well; flow ,2 gallons per minute; 
water rises 2 feet above ground; temperature, 70°. 

Wells on Ullman pla.ee, owned by Mudhall Smith: No. 1, 4 1-2 mile.* 
southwest of Marion Junction; flow, 2 gallons per minute; water rises 
2 feet above surface; temperature, 70°. No. 2, on old mill site, one-hal) 
mile east of No. 1, south of railroad; flow, 1 gallon per minute; wate* 
rises 2 feet above surface; temperature, 69°. No. 3, no record; does nox 
flow. All old wells. 

Will Moore's old wells: No. 1, 4 miles west of south of Marion Junc- 
tion; flow, 4 gallons per minute; water rises 3 feet above surface; tem- 
perature, 68° . No. 2, one-fourth miles east of No. 1; flow, 1 gallon per 
minute; water rises 2 feet above surface; temperature, 69°. Nos. 3 and 4; 
no record. 

Dave Taylor's wall, 5 1-2 miles south of Marion Junction; no record. 

Henry Stubbs's well, 5 miles southeast of Marion Junction, in Section 

33, Township 17, Range 9; bored in 1898 by Pat Gilmer; depth, 260 feet; 
water stands at —7 1-2 feet. Record: Soil, 0-8 feet; blue rock, 8-240 feec; 
rock, 240-242 feet; sand, 242-260 feet. Stopped in first water. 

Well on Crenshaw place, 5 miles south of Marion Junction, owned by Dr. 
Jones, of Selma; bored in 1904 by Gus. Somers; no record. 

Eulow well, 4 miles southwest of Marion Junction, in the N. E. quarter 
N. W. quarter Section 3, Township 16, Range 8; owned by J. W. Wallace, 
of Birmingham; flow, 1 gallon per minute; water rises 2 feet above the 
surface; temperature, 68°. 

Well on Woodruff place, 3 miles southwest of Marion Junction, Section 

34, Township 17, Range 8; owned by Mrs. S. E. Woodruff of Selma; old 
well; flow, 2 gallons per minute; water rises 3 feet above surface; tem- 
perature, 68°. 

Well on Bean place, 2 miles west of south of Marion Junction, in the 
S. W. quarter ' Section 26, Township 17, Range 8; o"wned by Dr. A. W. 
Jones, of Selma; flow, 2 gallons per minute; water rises 2 feet above 
ground; temperature, 69°. 

Well of Tom Harrell (colored), 2 miles southwest of Marion Junction, 
in the N. E. quarter Section 27, Township 17, Range 8; flow, 1 gallon per 
minute; water rises 3 feet above ground; temperature, 68 1-2°. 

Mrs. L. G. Port's wed, at station, Marion Junction; bored about 1890; 
depth, 250 feet; diameter, 3 inches; water stands at — 40 feet; pump used. 

The other wells at Marion Junction having the same record as Mrs. 
Fort's, are those of H. P. Randall, M. P. Smith, S. A. Brice, Dr. J. M. 
McDonald, C. E. Port, J. B. Moore, Mrs. M. P. Port, P. B. Harrell, and 
Pat Gilmore 

Sam Bryce's wells: No. 1, 3 miles northeast of Marion Junction, on 
north side of Marion Junction and Selma road, in the S. E. quarter S. E. 
quarter Section 7, Township 17, Range 9; old well; flow, 1 gallon per min- 
ute; temperature, 69°.' No. 2, in the N. E. quarter N. E. quarter Section 
7, Township 17, Range 9; old well; flow, 3 gallons per minute; wacer 
rises 3 feet above surface; temperature, 68 1-2°. 

Pennell wells, both old; No. 1 does not flow; No. 2 flows 3 gallons per 
minute; temperature, 70°. 

Reuben Tubbs's well, on Harrell place, 3 1-2 miles northeast of Marion 
Junction, in the N. E. quarter N. W. quarter Section 17, Township 17, 
Range 9; bored in 1860; depth, 250(?) feet; flow, 3 1-2 gallons per minute; 
water rises 3 feet above ground; temperature, 69 1-2°. 



WATERS OF THE CRETACEOUS. 203' 

W. A. Cochrane's well, one-fourth mile east of .!. Chisholm's well No. 
2; old well; How, one-half gallon pei minute; water rises 3 leet above 
surface; temperature, 00°. 

In addition to the above there arc in this neighborhood (north and 
northeast of Marion Junction) several wells which do not flow, on places 
belonging to S. H. White, on the Ward tract, and on the McCreary place. 
It may be remarked here that some of the wells credited to Perry County 
may be in Dallas, as they are close to the County line. 

Wells on Johnson place: No. 1, 1 3-4 miles southeast of Harrell's, 
in the S. E. quarter S. E. quarter Section 20. Township 17. Range 9; 
owned by J. \\ . Wallace of Birmingham; flow, 8 gallons per minute: 
water rises 3 feet above the ground; temperature. 09°. No. 2. 300 yards 
east of No. 1. estimated flow, 2 gallons per minute; temperature. 07°. 

Well on Moore place. 4 miles southeast of Harrell's in the N. W. quar- 
ter S. E. quarter Section 28, Township 17, Range 9; owned by E. L. Moor-?, 
of Marion Junction; old well; estimated flow, 15 gallons per minute; 
water rises 10 feet, above the surface; temperature, 09 1-2°. 

Well on Wade place (W. A. Cochrane estate), 3 miles southeast 'if 
Harrell's, in the S. W. quarter S. E. quarter Section 29, Township 17, 
Range 9; in a ravine S feet deep; old well; flow, 3 gallons per minute; 
temperature, 60 1-2°. 

Wells on Gill place: No. 1. 5 miles southeast of Harrell's, in the S. E. 
half S. E. quarter Section 3, Township 16. Range 9; flow, 1 gallon per 
minute; water rises 3 feet above the surface; temperature 08°. No. 2. 
50 yards north of No. 1, and on hillside 30 feet higher; flow, 1 gallon por 
minute; temperature, 68°. No. 3. in the S. E. quarter N. E. quarter Sec- 
tion 10, Township 16, Range 9; flow, 5 gallons per minute; water rises 2 
feet above the surface. 70°. All old wells. 

Well on Phil Milhous place. 1 mile a little east of south from Gill well 
No. 1, in the N. W. quarter N. W. quarter Section 11, Township 10, Range 
9; old well; estimated flow, 10 gallons per minute; water rises feet 
above the surface; temperature, 08°. 

Town well, Eleanor. S. W. quarter S. W. quarter Section 19. Township 
10. Range 8; bored by A. A. Simms in 1895; depth, 510 feet; casing, 3 1-2- 
inch; first water at 510 feet overflowed 1 1-2 feet above surface; original 
flow. 1 gallon per minute, 1 foot above surface; no longer flows. 

P. Walter Milhous's wells: No. 1, three-fourths mile west of Eleanor, 
in the S. half N. W. quarter Section 24, Township 10. Range 7; bored in 
1870; depth, 610 feet; diameter, 4 inches; flow, one-sixth gallon per min- 
ute; water rises 3 feet above the ground; temperature. 70 1-2°. No. 2, 
1 1-4 miles northwest of Eleanor, in the N. W. quarter N. E. quarter Sec- 
tion 24, Township 16. Range 7; bored about 1880; depth. 450 feet; diameter 
4 inches; flow, one-half gallon per minute; water rises 3 feet above sur- 
face; temperature, 70°. No. 2 well is about 25 feet higher than No. 1. 

J. N. Walker's well, one-fourth mile east of Eleanor, in the S. E. quarter 
S. W. quarter Section 19. Township 16, Range 8; old well; depth, 525 feet; 
casing. 4-inch; flow. 1 gallon per minute; water rises 1 foot above sur- 
face; temperature, 69°. 

Well on Josh Hurt place in the N. W. quarter N. E. quarter Section 
5, Township 16, Range 8; flow, one-fourth gallon per minute; tempera- 
ture. 72°. 

Wells on Chambers place: No. 1, in the S. &. quarter N. W. quarter 
Section 8, Township 16, Range 8; flow, 4 gallons per minute; temperature, 
70°. Nos. 2 and 3 are near No. 1 and ceased flowing a number of years 
ago. All are old wells. 



204 DETAILS : COASTAL PLAIN DIVISION. 

Well on King- place, S. E. quarter S. W. quarter Section 18, Township 
16, Range 7; owned by Mr. Potter; flow, 3 gallons per minute; water rises 
3 feet above the surface; temperature, 73°. 

Well on Roscoe place; old well: flows very weak stream, no record avail- 
able. Well on Hempshaw place, 1 1-2 miles west of Boguechitto; flow 2 
gallons per minute; water rises 4 feet above ground; temperature, 71°. 

Wells on Moss Grove place, 4 miles west of Boguechitto; owned by Col. 
S. W. John. No. 1, flows, 1 gallon per minute; temperature, 70 1-2°. No. 
2, three- fourths mile west of No. 1; bored by ^r. Potter in 1883; depth, 
1000 feet; casing, 4-inch; flow, 10 gallons per minute; first water at 520 
feet, stand — 18 feet; second water at 740 feet, stand — 11 feet; third water 
at 1000 feet, stand 8 feet above surface. 

Record of well No. 2, on Moss Grove Place, near Bougechitto. 



Feet. 

Soil 0— 22 

Blue rock 22 — 518 

Rock 518 — 520 

Sand and water 520 — 739 

Hard rock 739 — 740 

Sand 740 — 799 

Sand rock 799 — 1000 



No. 3, 1 mile west of No. 1; flow, one half gallon per minute; water 
rises 2 feet above the ground; temperature, 71°. No. 4, 1 1-4 mile north- 
west of No. 1; flow, 3 gallons per minute; water rises 3 feet above the 
surface; temperature, 71°. No. 5 and 6 are decreasing in flow, in decay. 

Dr. E. B. Moseley's wells: No. 1, one-fourth mile west of Boguechitto, 
in the S. E. quarter S. E. quarter Section 7, Township 16, Range 8; old 
well; no longer flows. No. 2, 150 yards west of No. 1, in the S. E. quarter 
S. E. quarter Section 7, Township 16, Range 8; bored about 1845; flow. 
1 gallon per minute; water rises 4 feet above ground; temperature, 71 a . 
No. 3, one-fourth mile east of No. 1, in the N. E. quarter N. W. quarter 
Section 17, Township 16, Range 8; bored by a negro in 1893; depth, 740 
feet; flow, 3 gallons per minute; water rises 3 feet above the surface; 
temperature, 71°. 

Well on William Moore place, 2 1-2 miles northeast of Boguechitto; old 
well; no longer flows. 

Well on Strong Johnson place, 1 1-2 miles northeast of Boguechitto; 
old well; no longer flows. 

Well on Wilson place, 2 miles west of Boguechitto; flow, 2 gallons per 
minute; water rises 4 feet above surface; temperature, 71°. 

Well on Carmichacl place, Elias Gray present owner, 3 miles west of 
Boguechitto; old well; flow, 1 gallon per minute; water rises 3 feet above 
ground; temperature, 71°. 

W. N. Carson's well, on Old's place, 1 1-2 miles south of Boguechitto; 
in the W. half N. W. quarter Section 20, Township 16, Range 8; flow, 
8 gallons per minute; water rises 3 feet above surface; temperature, 70°. 

E. M. Overstreet's well, 1 1-2 miles north of Boguechitto, in the E. 
half N. E. quarter Section 5, Township 16, Range 8; flow, 2 gallons per 
minute; water rises 3 feet above surface; temperature, 70°. 

W. N. Carson's well, 3 miles southeast of Boguechitto; in the N. LO. 
half N. E. half Section 28, Township 16, Range 8; bored about 1894 by 



WATERS OF Tin: CRETACEOUS. 205 

negroes; depth. 420 feet; casing, l-inch; Mow, i gallon per minute; water 
rises 2 feet above surface, temperature, 69°. Record: Clay, 0-30 feet; 
blue rock, 30-400 feet. 

.Mrs. Rainey's well, 1 1-2 miles east of Boguechitto, in the S. E. quarter 
S. E. quarter Section 16, Township 16, Range 8; flow, one-half gallon per 
minute; water rises 2 feet above surface; temperature, 70°. 

Bill Hatch's well, three-fourths mile southeast of Boguechitto, in the 
S. E. quarter S. W. quarter Section 17, Township 16, Range 8; flow, 4 
gallons per minute; water rises 3 feet above surface; temperature, 70°. 

George Washington's well, one-half mile west of south of Boguechitto, 
in the N. W. quarter S. E. quarter Section 18, Township 16, Range 8; 
bored in 1882; depth, over 400 feet; diameter, 4 inches; flow, 3 gallons per 
minute; water rises 3 feet above the surface; temperature, 71 1-2°. 

John Moore's well, three-fourth mile south of Boguechitto, in the N. 
W. quarter N. W. quarter Section 17, Township 16. Range 8; depth, 175 
feet; diameter, 4 inches; flow, 3 gallons per minute; water rises 3 feet 
above surface; temperature, 70°. 

Well on Adam Edwards place, cne-half mile south of Boguechitto, 
in the N. E. quarter S. E. quarter Section 18, Township 16, Range N; 
bored, in 1879; depth, 475 feet; diameter, 4 inches; flow. 3 gallons per min- 
ute; water rises 3 feet above surface; temperature, 70°. Record: Clay, 
0-14; blue rock, 14-470 feet; sand rock, 470-476 feet; overflows at 476 feet. 

Well on Sydney Edwards place, three-fourths mile north of east of 
Boguechitto, in the S. W. quarter Section 9, Township 16, Range 8; flow, 
2 gallons per minute; water rises 3 feet above ground; temperature, 69°. 

Wells on Dedman place, 1 mile north of Boguechitto: No. 1, in the 
E. half N. E. quarter Section 5, Township 16, Range 7; flow, one-third 
gallon per minute; water rises 4 feet above surface; temperature, 70°. 
Nos. 2 and 3 no longer flow. 

Andrew Ridgeway's well, on Harvey Hurt place, in the N. E. quarter 
N. W. quarter Section 5, Township 16, Range 7; water barely flows. On 
this place are two other wells; both old and no longer flowing. 

Wash Smith's well, Boguechitto, in the S. E. quarter S. W. quarter 
Section 6, Township 16, Range 8; flow, 2 gallons per minute; water rises 
4 feet above surface; temperature, 72°. 

Ebo Smith's well, three-fourths mile northwest of Boguechitto, in the 
S. E. quarter N. W. quarter Section 7, Township 16, Range 8; flow, one- 
fourth gallon per minute; water rises 1 foot above well mouth; tempera- 
ture, 69°. 

EAST OF Ai.AI'.AJIl IUVEE. 

Well on Watts place, 4 miles west of Sardis; owned by John Stanfleid; 
flow, 15" gallons per minute; water rises. to 4 feet above surface; tempe- 
rature, 72°. 

Well on Duke place. 4 1-2 miles west of Sardis; owned by W. W. 
Burns of Selma; flow, 2 gallons per minute; water rises to 4 feet above 
surface; temperature, 72°. 

Well on Stevenson place, 5 1-2 miles southwest of Sardis; owned by 
W. J. Stevenson of Berlin; flow, 1 gallon per minute; water rises to 12 
feet above surface; temperature, 74°. 

Wells on Reese place: No. 1, at Kings Landing, in the N. E. quarter 
S. E. quarter Section 20, Township 15, Range 10; estimated flow, 75 gal- 
lons per minute; water rises to 7 feet above the surface; temperature. 



206 details: coastal plain division. 

76°. No. 2, in the N. W. quarter N. E. quarter Section 29, Township 15, 
Range 10; estimated flow, 30 gallons per minute; water rises to 15 above 
the ground; temperature, 77°. 

Well on Middle place, 3 miles west of Kings Landing, in the N. E. 
quarter S. E. quarter Section 23, Township 15, Range 9; owned by Mrs. 
M. E. Reese, of Berlin; flow, 12 gallons per minute; temperature, 76 1-2°. 

Well on Wood place, 3 1-2 miles southwest of Kings Landing, in the 
S. E. quarter N. E. quarter Section 27, Township 15, range 9; flow, 30 
gallons per minute; water rises to 5 feet above the surface; tempera- 
ture, 76 1-2°. 

Well on Molette place, 3 1-2 miles southwest of Kings Landing, in -the 
N. W. quarter N. E. quarter Section 1, Township 14, Range 9; flow, 10 
gallons per minute; water rises to 3 feet above surface; temperature, 
77 1-2°. 

Well on Milhous place, 2 1-2 miles southwest of Kings Landing, in the 
S. W. quarter N. E. quarter Section 36, Township 15, Range 9; flow, 10 
gallons per minute; water rises to 3 feet above the ground; temperature, 
77°. 

Well on Creek place, 2 1-2 miles southeast of Kings Landing; Sec- 
tion 33, Township 15, Range 10; flow, 40 gallons per minute; water rises 
to 6 feet above the ground; temperature, 77°. 



LOWNDES COUNTY. 
Surface Features. 

The geological structure of Lowndes County is quite similar 
to that of Dallas County on the one side and Montgomery 
County on the other, and the conditions of water supply are 
practically the same. Very few well records, however, have 
been obtained from Lowndes County. 

The outcropping Cretaceous rocks are the Selma chalk in 
the northern part of the County and the Ripley formation in 
the southern. Both of these are mantled by the pebbles and 
red loam of the Lafayette. The interstream areas are high, 
flat table-lands', covered by the Lafayette deposits, where the 
best of the freestone water is obtainable from shallow wells 
and hillside springs. 

Throughout the northern half of the county the conditions 
for artesian wells should be favorable, but in the southern half 
the borings would necessarily be very deep, since they would 
have to pierce the entire thickness' of the Selma chalk. 

The Ripley beds form a belt 5 or 6 miles wide along the 
southern border of the county. They are composed of cal- 
careous sands interstratified with- limestone ledges. This ar- 
rangement of the strata, produces, in the process of denuda- 
tion, a very uneven and rugged country. In other counties 



WATERS OF THE CRETACEOUS. 207 

very few wells have been bored in territory formed by the 
Ripley beds, and the writer knows of none in Lowndes County. 

Aktksian Records. 

The following are the records for the entire county. 

SCOTT HILL. 

W. D. McCurdy's well, 4 miles west of Lowndesboro, on a high hill; 
bored by Bicksler in 1903; water stands at —140 feet; boring ends prob- 
ably in Tuscaloosa beds. 

Record of W. D. McCurdy's well, Scott Hill. 



Feet. 

Clay — 40 

Blue rock 40 — 475 

Hard rock 475 — 477 

Sand 477 — 525 

Blue marl 525 — 575 

Rock 575 — 578 

Soft sandstone 578 — 625 

Quicksand 625 — 680 

Blue clay 680 — 700 



LOWNDESBOPO STATION. 

C. M. Smith's well bored by A. Ockenden in 18S9; depth, 700 feet; cased 
to bottom with 2-inch, 3-inch, 4-inch casing; water stands at — 23 feet; 
4000 gallons have been pumped out in a day without lowering the level; 
does not flow; first water at 150 feet, stand —75 feet, salty; second water 
at 450 feet, stand —75 feet; third water at 700 feet, stand —23 feet; boring 
probably ends in Tuscaloosa beds. 

Record of C. M. Smith's well, Loivndesooro Station. 



Feet. 

Clay and gravel — 15 

Blue rock 15 — 150 

Sand 150 — 155 

Clav 155 — 450 

Sand 450 — 455 

Clay and sand 455 — 700 



CORKIE. 

T. J. Hairston's well, in Section 17 or IS, Township 14, Range 16 B; 
bored by Ingraham; depth, 562 feet; water stands at —80 feet; raised by 
Marsh steam pump, delivering 2 1-2 gallons per minute; it is thought 
that a larger pump would not exhaust or lower the water; water has 
a decided taste, thought to be of soda. 



208 details: coastal plain division. 

HAYNEVILLE. 

One well 800 feet deep; water stands at — 80 feet; raised by steam 
pump. 

MONTGOMERY COUNTY. 
Surface Features. 

Montgomery County lies altogether within the limits' of the 
Cretaceous beds. The Eutaw division, consisting of yellowish 
and reddish cross-bedded sands with clay partings, is well 
exposed in the railroad cuts and along the river bank at 
Montgomery, and occupies that part of the county east of the 
city lying between Alabama River on the north and the line 
of the Central of Georgia Railway on the south. In the lower 
townships of the county the strata of the Ripley occupy the 
surface, while all the intermediate area is underlain by the 
Selma chalk. 

Shallow Waters. 

In the Eutaw and Ripley territories the sandy strata serve as 
water-bearers, and in all three divisions the overlying Lafay- 
ette sands, pebbles, and loams still remain in places on the di- 
vides, making level plateaus about 400 feet above tide level. 
In the Lafayette areas an abundant supply of good water is 
obtained from wells and springs. As is the case elsewhere, 
the Selma chalk, or "rotten limestone," is unfavorable to the 
existence of good surface waters and consequently the great- 
est number of artesian wells are found in the area of its out- 
crop. 

While the strata of the Tuscaloosa formation do not appear 
at the surface within the limits of Montgomery County, they 
outcrop in the bordering counties of Autauga and Elmore, and 
undoubtedly underlie the Eutaw sands south of Alabama River. 

Artesian Records. 

The southern limit of the Selma chalk area in Montgom- 
ery County is marked by an infacing escarpment, or a range 
of hills with steep and abrupt northward slopes, but gentle 
slopes toward the south. This escarpment marks' also the Vim 



WATERS CM? THE CRETACEOUS. 209 

between lands on the north depending for water supply on ar- 
tesian wells, and those on the south in which the sands hold 
sufficient water to supply all ordinary needs. 

No record of any artesian borings south of this' line has been 
found, and in this respect Montgomery County agrees with all 
the other counties similarly situated geologically. 

Of the wells whose records are given below, the following are 
located on the Eutaw sands and get water either from these 
or from the underlying Tuscaloosa materials : Well on place 
formerly owned by M. E. P'ratt, at Pratt Ferry; most of the 
wells' in the city of Montgomery ; wells on Martin Baldwin 
place and Paul Le Grand place, north of Montgomery. 

The well records from the city of Montgomery have been 
most carefully kept and give the most information, and they 
are given first. 

MONTGOMERY. 

Within the memory of many now living the old wells in 
Exchange square and on Commerce street yielded overflowing 
streams ; but the recent sinking of so many large wells within 
the city limits has so lowered the water table that neither of 
these now flows and the same is probably true of all the older 
s'mall w-ells. Of the older wells of the city waterworks, the fol- 
lowing was bored by William D. Chapin : 

Record of Chapin well of City Waterworks, Montgomery. 

Feet. 

Clay 30 

Sand and gravel 60 

Sand rock, full of hard nodules 6 

Black clay that flakes off like slate on exposure to 

the air and turns gray 4 

So-called marl with streak of clay 80 

Sand with water, but not a running sand; more like 

a very soft sandstone 20 

Marl and clay 100 

Sand with water, like second above 15 

Marl and clay 80 

Coarse sandstone, some water, very soft 25 

Hard sandstone, large flow of water, rises about 25 feet 

above the surface 2 

Clay and marl, with a hard streak of lime rock at bottom 90 

Lignite 3 

Marl in loose pieces, like stones on seashore 60 

Clay 5 

Very hard lime rock 2 

Coarse white sand, with streaks of hard sandstone; large 

flow of water, say 200 gallons per minute, rises about 

40 feet above surface 51 

633 

14 



210 



DETAILS : COASTAL PLAIN DIVISION. 



Below this to the bottom of the boring was marl. The marl in this 
boring is probably a fossiliferous sand with streaks or partings of clay. 
While the boring undoubtedly reaches the strata of the Tuscaloosa for- 
mation, it is impossible from the record to say where the transition 
from the Eutaw sands to the Tuscaloosa occurs. It is probably some- 
where between 250 and 300 feet. 

The books of the city waterworks contain much information concern- 
ing artesian conditions in Montgomery. Previous to 1899 there were six 
wells in use, the Cook, Parker's West, South, Northwest, Southwest, and 
Southeast wells, all bored by the CoOk Well Company, of Chicago, 111. 
Twelve new wells were sunk in 1899. These wells do not flow and airlift 
is necessary. It is estimated that the daily capacity, when all are con- 
nected, is 5,000,000 gallons. The average temperature is 68°. The record 
of the Cook and Parker's West wells and some details of the four other 
older wells are given below. 

Old Cook well, depth, 837 feet; started with 12-inch casing; flowed 
191,998 gallons m twenty-four hours when well was first started. 



Record of Cook well, Montgomery. 



Feet. 

White clay — 16 

White sand 16 — 18 

Blue marl 18— 26 

Coarse gravel; washing water would not fill well; had to use 

sand pump 26— 55 

Coarse gravel 55 — 8o 

Blue marl; stopped the 10-inch casing, as it would not drive; 

substituted 8-inch casing; struck fine gravel and sand 85 — 139 

Blue marl; water stood at — 10 feet, sand rock at 145 feet 18 

inches; no headway drilling, used rotary process 139 — 145 

Thin blue clay 148 — 170 

Fine white sand 170 — 188 

Blue clay 188 — 2z5 

Light yellow sand 225 — 240 

Red clay 240 — 255 

Blue clay and sand i 255 — 258 

Red clay 258 — 280 

Yellow sand 280 — 288 

Blue clay 288 — 297 

Sand and clay 297 — ::l2 

Clay 312 — 320 

Red and blue clay; water flowed 8 feet above surface 320 — 345 

Clay 345 — 365 

Coarse water-bearing sand 365 — 373 

Lignite in sand, with 1 1-2-inch rock 373 — 3^0 

Sand rock and sand, cavity 6 feet 380 — 388 

Water-bearing sands 388 — 402 

Fine sands 402 — 410 

Sand, with ledges of sand rock 410 — 421 

Clay and sand ; some water 421 — 450 

Finer sand, with a little clay 450 — ' 4S0 

Fine sand; some red, mixed with clay 480 — 507 

Black clay 507 — 530 

Sand 530 — 540 

Black clay, with traces of sand 540 — 585 

Sand and clay 585 — 610 

Very fine, water-bearing sand; temperature, 70° 610 — 650 

Blue clay, with some yellow 650 — 720 

Blue and red clay 720 — 837 

837 



WATERS OF THE CRETACEOUS. 211 

Record of Parker's West well, Montgomery. 



Feet. 

Sand and gravel — 89 

Clay so— 109 

Clay and sand 109— 129 

Fine and coarse sand 129 — 178 

Sand and blue mail 178— 185 

Clay and sand 185— 225 

Red clay and sand 225— -J30 

Sand: hole, caved 40 feet; water overflowed a little 330— 395 

Sand 395— 471 

Black clay 471— 507 

Black clay, with some sand; good stream 507 — 53U 

Black clay 530— 546 

Sand 546 — 580 

Blue clay 580— 585 

Sand, with very little clay; water to surface at COO feet 585— 621 

"White sand 621 — 652 

Stiff clay 652— 662 

White sand 662 — 706 

Red sand ; some clav 706 — 714 

White sand 714— 785 

Reddish sand 785— 7y5 

White sand 795— 837 

Sand and clay S37 — fl6 

White sand 876— 880 

White sand and clay 880 — 88S 

White sand and beds of clay and sand 888 — 895 

Hard sand rock, some white, alternating - with softer rock 895 — 1091 



"Water rises 200 feet. Salt water at 1091 feet, in reddish clay. Stopped 
drilling at this point. Cased off at 712 feet, using water found at that 
point. Water from this well pumped into Cook well. 

South well, depth, 650 feet. 

Northwest well, depth, 457 feet; 340 feet 8-inch casing, 67 feet 6-inch ca- 
sing, 50 feet 6-inch strainer; flow, 92 gallons per minute. 

Southwest well, depth, 448 feet; 338 feet 8-inch casing, 60 feert 6-inch cas- 
ing, 50 feet 6-inch strainer; flow, 60 gallons per minute. 

Southeast well, depth, 645 feet. 

A number of tests have been made by means of airlift to determine 
the capacity of the different wells. These have varied somewhat at 
different times. The following are probably typical: 



Capacity of wells at Montgomery, as shown by air-lift tests. 



. Gallons per Gallons per 

Well. . minute. 24 hours. 

Northeast well 285 410,400 

Southwest well 212 304,280 

Cook well 225 , 324,000 

Parker well 239 344.160 

961 1,383,840 
In 18S9 12 new wells were bored for the waterworks company, i 
the record given below. 



2L2 details: coastal plain division. 

Record of new waterworks wells, Montgomery. 



Feet. 

Top soil 0— 15 

Clay 15— 95 

Marl 95 — 225 

Water-bearing sands 225 — 228 

Reddish clay with pebbles; small ledge of 

sandstone 228 — 450 

Black clay ; water 450 — 650 



At 650 feet the water stood at —20 feet; at 450 feet, —35 feet; and at 21i0 
feet. —50 feet. As has been said above, on account of the many wells 
sunk in Montgomery the water now stands much lower than formerly. 

In the records given the red clays of the Tuscaloosa formation appear 
to have been reached at depths of 225 to 250 feet, which is about what 
one would anticipate from tne horizon of the mouth of the wells, which 
is about 100 feet below the top of the Butaw sands. 

Other records of wells in Montgomery are as follows: 

Well at Exchange Hotel, bored for D. P. West, proprietor; depth, 650 
feet; casing, 2-inch and 4-inch; water stands at — 45 feet; temperature, 
66°; good drinking water, but not fit for boilers. 

Analysis of water from well at Exchange Hotel, Montgomery* 



Parts per million. 

Sodium (Na) 78.70 

Potassium (K) 16.21 

Magnesium (Mg) .38 

Calcium (Ca) 4.32 

Chlorine (CI) 7.66 

' Sulphuric acid (SO*) 1.50 

Carbonic acid (HCO s ) 144.13 

Iron (Pe) Trace. 

Silica (Si0 2 ) 11.81 

264.71 

Montgomery Brewery wells: No. 1, depth, 550 feet; temperature, 68°; 
sand and a little water at 90 feet; cased off and lowered to 480 feet, 
passing through blue clay and sand; some water, supply insu..cient; 
lowered to 550 feet, reaching good water with a flow 6 feet above the 
surface. No. 2, depth, 700 feet; passed through sand and blue clay, 
with ledges of rock 2 feet thick; cased to 550 feet; supply inexhaustible; 
stands now at —17 feet, on account of stream being turned into well No. 
1. 

Montgomery Ice and Storage Company's well, bored by Tillison in 
1903; depth, 163 feet; casing, 6-inch; first water at 35 feet, stand —35 feet; 
second water at 140 feet, stand —27 feet; 100 gallons per minute pumped 
from this well constantly. Record: Clay, 0-30 feet; sand, 30-38 feet: 
gravel, 38-50 feet; sand and water, 50-94 feet; soapstone with sand, 94-140 
feet; sand, gravel and water, 140-160 feet. The well of the Union Slaugh- 
terhouse, 600 yards east of this well, encountered no gravel. 

*Expressed by analyst in grains per gallon and hypothetical combi- 
nations ; recomputed in ionic form and parts per .million at U. S. 
Geological Survey. 



WATERS OF THE CRETACEOUS. 2J3 

Union Slaughterhouse well, bored by Tillison in 1898; depth, 1G3 feet, 
first water at 20 feet, stand —20 feet; second water at 140 feet, stand —23 
feet. Record: Clay, 0-20 feet; sand, 20-110 feet; soapstone, 110-140 feet; 
sand and water, 140-163 feet. 

NORTH AM) WEST OF MONTGOMERY. 

The thiee wells n^xt feiio-virg are also ou the T^dtaw sand;;: 

Well on old Jesse Cox place, afterwards owned by M. E. Pratt, at 

Pratt's Ferry, 10 miles west of Montgomery; bored by Wm. D. Chapin; 

overflows. 

Record of well on old Jesse Cox place, Pratts Ferry. 



Feet. 

Clay 0— 20 

Sand and gravel 20 — 30 

Marl 30— 35 

Tough black clay 35 — 65 

Marl 65 — 265 

Sand, with streaks of sandstone, water- 
bearing 265 — 320 



The material called marl in the above record is the same as that which 
makes the lower part of the bluff at the ferry on the opposite side of 
the river; it consists of cross-bedded calcareous sands with a few fos- 
sils and is interstratified with tough laminated black clays. This is 
called marl at Prattville and elsewhere. All the strata penetrated by 
this boring belong to the Eutaw formation. 

Well on Martin Baldwin place, 7 miles north of Montgomery, in the 
S. W. quarter Section 8, Township 17, Range 18; bored by M. S. Gilmer 
in 1898; flow. 3 gallons per minute; water rises to 2 feet above the surface: 
temperature, 67°. 

Well on Paul Le Grand place, 4 1-2 miles north of Montgomery; bored 
by Sarber in 1904; depth, 423 feet; casing, 2-inch. 

First water at 115 feet, stand — 45 feet; 

Second water at 200 feet, stand — 23 feet; 

Third water at 300 feet, stand —15 feet; 

Fourth water stand —15 feet: 

Record: Clay. 0-20 feet; clay and compact dry sand, 20-115 feet; (?) 115-200 
feet ; sand and water, 200-210 feet; clay and compact sand. 210-300 feet; 
sand and clay, 300-423 feet. 

SOUTH AND EAST OF MONTGOMERY. 

South of the line of contact of the Eutaw and Selma chalk 
outcrops, artesian water is obtained from the sands of the Eu- 
taw at varying depths. Comparatively few of these wells yield 
flowing water, and it is reported by Mr. F. J. Tillison, who 
during the last twenty-five years has bored at least a hundred 
wells in the county, mainly in the northern half, that only five- 
are overflowing wells. These are the following: 



214 details: coastal plain division. 

Well at Abraham Church, 4 miles south of Montgomery, in the S. E. 
quarter Section 36, Township 16, Range 17; diameter, 4 inches; flow, one- 
fourth gallon per minute; water rises to 1 foot above surface; tempera- 
ture, 69°. 

Griel Brothers' well, on Forbes place, 5 miles south of Montgomery, in 
the N. E. quarter Section 1, Township 15, Range 17; depth, 86 feet; water 
stands at surface. 

Silas Tyson's wells, 4 miles west of south of Montgomery, in the S. E. 
quarter Section 35, Township 16, Range 17: No. 1, in field; depth, 60 feet; 
flows; temperature, 66°. No. 2, in pasture; water stands at 2 feet above 
surface; makes a kind of cistern. 

W. E. Pierce's well, 4 1-2 miles west of south of Montgomery, in Sec- 
tion 2, Township 15, Range 17; depth, 65 feet; flow, 2 1-2 gallons per min- 
ute; water rises to 3 feet above surface; temperature, 66°. 

The other records from Montgomery County are given as nearly as 
practicable in order from west to east. 

Well at Stone's on the Western Railway of Alabama, 7 or 8 miles west 
of Montgomery; new well; flow, about one-eighth gallon per minute; 
temperature, 72°; no other record obtained. 

A. H. Clark's wells, Hope Hull: No. 1, at house one-half mile east 
of postoffice; bored by Tillison in 1894; depth, 265 feet; casing, 4-inch; 
first water at 250 feet, stand —75 feet. Record: ' Clay, 0-20 feet; marl, 
20-250 feet; sand and water, 250-265 feet. Five other wells; records not 
available. 

Well of Atlantic Coast Line railroad, Sprague Junction; bored by Tilli- 
son in 1892; depth, 738 feet; casing, 4-inch; first water, at 645 feet, stand? 
at — 75 feet; tastes strong of soda. Record: Sand and clay, 0-16 feet; 
marl, 16-645 feet; sand and water, with occasional rock, 645-738. 

Another well at Sprague Junction is reported to be 400 feet deep, with 
8-inch and 6-mch casing; water stands at — 75 feet; no record obtained. 

In connection with the record of the railway well at Sprague Junc- 
tion given above. Mr. Tillison reports that Conover bored another 
20 feet away from the first, going down 1100 feet, casing to 900; but 
the water rose no higher than —75 feet. It could not be used in the 
boilers. 

Mr. Tillison reports further that in Montgomery county the first, third 
and fourth waters of Mr. Hawk, as explained on page 113, all rise to the 
same height. As a rule Mr. Tillison does not case below the marl, 
which may be the explanation of this circumstance. 

Dr. J. M. Galloway's well, 1 mile northeast Oi. Snowdoun; bored by 
lillison in 1891; depth, 527 feet; diameter, 4 inches; water stands at —80 
feet; first water at 510 feet. Record: Clay, 0-20 feet; marl, 20-360 feet; 
sand and water, 360-380 feet. 

Amos Jones s well, 16 miles from Montgomery (6 miles east of south); 
bored by Tillison in 1879; depth, 527 feet; water stands at —80 feet; first 
water, at 510 feet, stood at —80 feet. Record: Clay, 0-20 feet; marl, 20-510 
feet; sand and water, 510-527 feet. 

According to F. J. Tillison a well at Barachias is 200 feet deep and 
the water scands at — 16 feet, and the same authority states that a well 
at Myrtle is 250 feet deep, with the water standing at — 20 feet. 

P. H. Hammack's well, Pike Road; bored by Tillison in 1895; depth, 
352 feet; casing, 4-inch; first water, at 340 feet, stands at — 95 feet. Record: 
Sand, 0-20 feet; marl, 20-340 feet; sand and water, 340-352 feet. 

W. H. Lawson's well, near Mitchell Station, but in Montgomery County; 
bored by Y. T. Radford in 1899; depth. 680 feet; casing, 4-inch; first water 
at 630 feet, stand —50 feet. Record: Soil, 0-20 feet; marl, 20-630 feet; hard 
rock, 630-631 feet; sand, 631-680 feet. 



WATERS OF THE CRETACEOUS. 215 

AUTAUGA COUNTY. 

Shallow Waters. 

The Tuscaloosa formation underlies the northern half of 
Autauga County and the sands and clays of the Eutaw the 
southern half. Over these rocks is spread the surface mantle 
of loam and pebbles of the Lafayette formation. The condi- 
tions are therefore favorable for a never failing supply of 
freestone water from springs and open wells throughout the 
entire county, and for artesian wells especially in the lower half, 
within the Eutaw territory. 

Artesian Prospects. 

Because of the abundance of springs, and the fact that good 
water can be obtained almost everywhere in the county by 
wells of moderate depths, it has been only within the last two 
years that attempts have been made to get artesian water, and 
the records of artesian wells are as yet confined to the lowlands 
of Autauga and Swift Creeks, at Prattville and Autaugaville. 
The stratigraphic conditions, however, are favorable in other 
parts of the county underlain by the Tuscaloosa beds. 

PRATTVILLE. 

The first attempts to get artesian water were made in Pratt- 
ville in the summer of 1904, Mr. Ira E. Sarber, of Thorsb\ . 
being the contractor. 

Prattville, is situated in the valley of Autauga Creek, the 
elevation being considerably less than 100 feet above high- 
water level in Alabama River, 4 miles away. It is stated that 
in 1894, on a place owned by Dr. Robert Davis, in Prattville. 
a well was driven about 30 feet deep, in which the water rose 
about 10 feet above the surface, and that it is still flowing, but 
rises only about 3 feet above the surface. About the sanu- 
time Mr. M. D. Fisher bored a well 100 feet deep, in which the 
water stood at the surface until the spring of 1904, when it 
rose 3 feet above the surface, and has flowed ever since. 

Since the spring of 1904 a great number of wells have been 
bored and the number is constantly increasing. As the records 
will show, water is commonly obtained at a depth of 100 feet, 



216 DETAILS: COASTAL PLAIN DIVISION. 

more or less, when the mouth of the well is approximately at 
the level of the Prattville streets. In cases where the depth is 
greater, it is generally because the elevation of the well is 
higher, as at Mrs. Pratt's and at Mr. Daniel Pratt's. 

The sands' first penetrated, to the depth of 20 to 30 feet, arc 
the comparatively recent sands of the Autauga Creek bottom, 
on which the greater part of Prattville stands. The marl re- 
ferred to in the records consists of alternations of calcareous 
sand and gray clays ; some of the strata contain shells by which 
the formation is easily identified as' Eutaw. 

Public well, at bridge; bored by I. B. Sarber, in July, 1904; depth, 99 
feet; casing-, 64 feet, 2-inch; flow, (Sarber) 20 gallons per minute; water 
rose in 1-inch pipe to 24 feet above surface; measured flow October 20, 
1904, from spigot, 12 gallons per minute. 

Li. L. Chapman's 'well; bored by Sarber in 1904; flow, 20 gallons per 
minute; at first, much sand; measured flow October 29, 1904, 30 gallons 
per minute; casing, 4-inch, 50 feet; temperature, 66°. Record: Sand, 0-28 
feet; marl (Eutaw), 28-79 feet; water sands, 79 feet to bottom, about 100 
feet. 

E. I. Smith's well, bored by Sarber in 1904; depth, about 100 feet; log 
similar to others in town; measured flow October 29, 1904, 25 gallons per 
minute. This well and Chapman's were the largest in town, until the 
well at the Baptist church was bored. 

Academy yard well, bored by Sarber in 1904; surface about on same 
level as at Dr. Rice's and Mr. Graham's; casing, 70 feet, 2-inch; flow 
(Sarber), 20 gallons per minute; water rises in 1-inch pipe to 13 feet 
above the surface; measured flow October 29, 1904, from 1-inch pipe, 12 
gallons per minute; temperature, 65°. Record: Sands, 25-30 feet; marl, 
30-90 feet; water-bearing sands, 90-99 feet. The following analysis win 
made by Mr. Hodges: 

Analysis of water from Academy well, Prattville. 



Parts per million. 

Potassium (K) 1.2 

Sodium (Na) 1-3 

Magnesium (Mg) .4 

Calcium (Ca) .6 

Iron (Be) .2 

Alumina ( A1 2 3 ) -3 

Chlorine (CI) 1-7 

Sulphuric acid (S0 4 ) -5 

Carbonic acid (HCO s ) 5.6 

Silica (Si0 3 ) 15.6 

27.4 



details: coastal plain division. 2i7 

Sanitary Analysis. 



Parts per million. 

Nitrogen as 

Free ammonia 0.01 

Albuminoid ammonia None. 

Nitrates .02 

Nitrites None. 

Chlorine 1.7 

Total residue 19. 

Loss on ignition 7.4 



W. M. Fisher's well, bored by Sarber in 1904; depth, about 90 to 95 
feet; flow, 6 to 8 gallons per minute; log similar to others. 

Dr. Clarence Rice's well, bored in July. 1904, by Sarber; casing, 70 
feet, 2-inch; first water at 55 feet, rising to — 7 feet; second water, first 
overflow, at 100 feet; flow at first, 8 gallons per minute, increasing in 
three or four weeks to 20 gallons; water rises in 1 1-2-inch pipe to 16 
feet above surface. Record: Sands. 0-30 feet; marl, 30-55 feet; water- 
bearing sands, 55-62 feet; marl, G2-100 feet; water-bearing sands, 100-115 
feet. 

Malcolm Graham's well, bored in July, 1904, by Sarber; record same as 
that of Dr. Rice's well but depth is 123 feet. The surface here is 2U 
to 25 feet higher than at the bridge. Flow (Sarber), 15 gallons per min- 
ute; measured flow October 29. 1904. from one-half inch pipe, about ft 
gallons per minute. 

J. C. Burns's well, bored in July. 1904. by Sarber; casing, 60 feet, 2-inch 
water rose in 1-inch pipe to 20 feet above surface; flow, 20 gallons per 
minute, decreasing after six months to 14 gallons; measured flow Octo- 
ber 29, 1904, 12 gallons per minute. Record: Sand, 0-23 feet; marl, 23-23 
feet; sand, 28-37 feet; marl, 37-80 feet; water sands, with streaks of marl, 
80-94 feet. 

G. Cook Spigener's well, bored by Sarber in 1904; depth, about 86 feet; 
flow, 2 1-2 to 3 gallons per minute. 

Thomas Fay's well, bored by Sarber in 1904; water rose to 30 fecst 
above surface; flow, about 10 gallons per minute; temperature, 65°. 

Mr. Anthony's well, bored in November, 1904; flow, 1 gallon per minute. 
Daniel Pratt's well, bored in November 1904; flow 50 gallons per min- 
ute at first, decreasing to 12 gallons in three months and to 6 or 8 gallons 
in six months. Another well was bored later in the same yard. Record 
of No. 1: Sand, 0-30 feet; marl, 30-80 feet; coarse white sand (first water 
rising to —2 feet), 80-86 feet; marl, 86-108 feet; sands like those in town 
wells (second water, rising to 2 feet above surface), 108-116 feet; marl. 
116-120 feet; coarse sand and pebbles (third water, rising to 7 feet above 
surface). 120-126 feet; (?), 126-198 1-2 feet. 

Mrs. Julia A. Pratt's well, bored by Sarber in September, 1904; casing 
100-160 feet, 2-inch; first water below 100 feet, flowing 2 1-2 gallons per 
minute, cased off; second water at 180 feet; flow at nrst, 11 gallons per 
minute; decreasing after one week to 5 1-2 gallons, probably stopped by 
pebble. Record: Sands. 0-40 feet; marl. 40-140 feet; sand, 140-147 feet; 
marl. 147-180 feet; water-bearing sands. 180-198 feet. 

The following is a partial list of wells bored in Prattville and vicinity 
since the fall of 1904. It is almost impossible to keep up with the borings. 



218 details: coastal plain division. 

Wells bored in Prattville and vicinity since 1904. 

Bored by J. S. Catts, 1904-1906. 
Diameter, 2 inches. 



No. 



For whom drilled. 







§ 








rt 


to 


■-" Ol 


* 


n 


r— ! Q* 


a+j 






0) <D 






P^ 


£ to 



Stand. 



Jack Smith | 110 

Will Anderson | 103 

Mrs. Montgomery j 176 

Buford McKeithen 325 

Thornton place, (Thomas) 137 

Campbells place, (Thomas) 147 

Sim Fair place, (Thomas) 135 

Bulger place, (Thomas) 142 

Ice Factory, (Thomas) 152 

On Washington road, (Thomas) 158 

Ben Durden 139 

(1) Paradise, (Cotton mills) 146 

(2) Paradise, (Cotton mills).. 150 

(3) Paradise, (Cotton mills) .. 112 

(4) Paradise, (Cotton mills) .. 139 

Daniel Pratt 160 

Continental Gin Factory 157 

Mrs. Dora Barnes yard j 139 1 

Dr. Rice I 178 1 

Dr. Rice | 193 1 

Mrs. Pratt | 138 1 

Bob Golden | 120 1 

Ed. Golden | 100 1 

Mrs. Smith | 165 1 

Baptist church 165 1 

Bob Wards, (Thomas) | 1381 

Methodist parsonage [ 124 1 

J. W. Young . I 276| 

William Graham | 167 1 

William Graham | 1961 

Wade Hunt J 198 1 

Baptist parsonage ] 196 1 

Mrs. McCrary j 131 j 



4-5 
4-6 
lost 
4- 
6-8 
6-10 
3-4 
5-8 
25-30 
20-30 
8-10 
3-4 
15-20 
4-5 
3-5 
10-12 
6-8 
6-8 
lost 
160| 20-30 
120| 10-12 
98| 10-12 
65| 10-12 
140| 20-30 
142 | 100- 



60 1 

62 1 

120| 

250 

68 

60 

100 

87 

102 

110 

100 

10i» 

116 
96 

94 
110 

100 

108| 

■ I 



l\ 
86 1 

2201 
140 1 
1601 
163| 

1821 



4-6 
4-6 

lost 

4- 

5-6 

4-6 

4-6 



I Overflows. 
I Overflows. 
\ Struck cavity. 

(Pump) 150 feet. 

Overflows. 

Overflows. 

Overflows. 

Overflows. 

Overflows. 

Overflows. 

Overflows. 

Overflows. 

Overflows. 

Overflows. 

Overflows. 
| Overflows. 

Overflows. 

Overflows. 

Broke rod. 

Overflows. 

Overflows. 

Overflows. 

Overflows. 

Overflows. 
I Overflows. 

Overflows. 
I Overflows. 
I No stream. 
| Broke pump. 
1—100 foot Pump. 
|Overflow<=- 
| Overflows. 

Overflows. 



Mr. CaiLS gives as the average record of the wells drilled by him the 
following: Sand and a hard pan composed of very fine white sand, 
very hard, 20 feet; yellow or red clay or marl, with some fine beds of 
ochre, red and yellow, and a great deal of ising glass, 80-100 feet. 

The best streams are found in very coarse sand and gravel, which is 
forced out by the pressure of the water. From well No. 25 of the above 
list over a car load of sand came up. Only one well strong in lime, 
viz., No. 4. The water generally becomes clear in 2 to 10 hours. No rock 
struck in any of these borings, but some gravel in all. 

From other sources the following notes are obtained: 

L. Q. Nelson's well, Chestnut street crossing of Louisville and Nash- 
ville railroad. 

Well near - obile and Ohio railroad. 

Well in lot between W. F. Wilkinson's and Dan Smith's. 



WATERS OF THE CRETACEOUS. 219 

AH' Wadworth's well several miles south of Prattville, on the old 
Daniel Pratt plantation; depth, -'ill feet. 

Maj. M. M. Smith's well 3 miles southwest of Prattville; not flowing; 
stand of water, — 12 feet. 

John Wadsworth's well, bored by Shackelford in 1905; depth, 475 feet; 
casing. 254 feet, 2-inch, 445 feet 1 1-4-inch. Record: Red clay, 0-19 feet; 
gravel, 19-41 feet; sand rock 18 inches thick at 83 feet; fine-grained sand, 
with water, 104-107 feet, and 144-154 feet; rock 8 inches thick at 260 feet; 
water, 290-296 feet; coarse yellow sand, with water, rising to surface. 
435-440 feet; marl, chalk, and red and yellow ocher, 440-474 feet; at bot- 
tom of boring, 475 feet, water rising above the surface and flowing 15 
gallons per minute. 

AUTAUGA VILLE. 

Jim Nunn's well, 1 mile from Autaugaville; bored by Radford in 189S; 
depth, 200 feet; casing, 4-inch; first water at 180 feel, stand —100 feet; 
much gravel. 

ELMORE GOUN1Y. 

Surface Features. 

The northern part of Elmore County, as far south as We- 
tumpka and Tallassee, is underlain by the metamorphic 
gneisses and mica schists ; southward from that latitude to Tal- 
lapoosa River, which separates Elmore from Montgomery 
County, the strata are Cretaceous', ranging from the Tuscaloosa 
to the lower measures of the Selma chalk. In the southern 
part of the county, below Wetumpka and east of Coosa 
River, and in all that part lying west of the Coosa and 
its continuation in the Alabama, the older rocks are covered 
with with the Lafayette mantle of pebbles and red loam. Dis 
continuous remnants of this mantle are also to be found in 
places on the east side of the Coosa, lapping far up over the 
metamorphic rocks. 

Shallow Waters. 

Where the Lafayette mantle is absent the residual soils and 
other materials from the crystalline rocks constitute the water 
reservoir and the supply from springs and wells is not always 
satisfactory, though generally adequate. On the other hand, 
wherever the Lafayette loam and pebble beds cover the surface 
the best freestone water is abundant. West of Alabama and 
Coosa rivers to the borders of Autauga County and beyond, 
relatively low lands of unusually level surface extend from op- 



220 details: coastal plain division. 

posite Montgomery practically to the line of Chilton County. 
In all this territory the Lafayette materials form the surface, 
and on each side of these lowlands, which are followed by the 
Louisville and Nashville Railroad, flat-topped hills capped 
with the same materials rise to elevations of ioo feet or more 
above the railroad. On closer examination of these hills the 
sands and clays of the Tuscaloosa formation may usually be 
discovered underneath the Lafayette beds. As in other coun- 
ties, the plateaus capped by the Lafayette beds form the finest 
farming lands of the region. 

On the borders of the lowlands mentioned is the town of 
Robinson Springs, so called from the fine springs which emerge 
from below the Lafayette pebble beds at their contact with the 
less pervious' Tuscaloosa clays. This water is similar to that 
of all the Lafayette springs, an analysis of one of which, the 
University Spring, is given under Tuscaloosa County, (p. 116). 

South of Wetumpka, in the N. E. quarter Section 18, Town- 
ship 18, Range 19 E., is the Harrowgate Sulphur Spring, 
once a famous place of resort, but now entirely abandoned. 
This spring is in the low grounds of a small stream running 
into the Coosa, and it is difficult to determine the bed from 
which it comes though it is probably one of the lower Cretace- 
ous formations. Sands have washed over the site of the 
springs and the buildings have been allowed to> fall into decay, 

Artesian Conditions. 

In the territory of the crystalline schists the conditions are. 
as a rule, unfavorable for artesian waters, though deep borings 
will almost anywhere fill with water to within pumping distance 
of the surface, and in many cases with a fairly good supply. 

In the area west of Alabama and Coosa rivers and south of 
Wetumpka on the east side of the Coos'a, the prospects for ai - 
tesian wells are more favorable because of the underlying 
Cretaceous (Tuscaloosa) beds. As yet few artesian borings 
have been made. The available records are given below. 

PEATTVILLE JUNCTION. 

Well in S. E. quarter N. B. quarter Section 10, Township 17, Range 17; 
bored by Sarber in 1904; depth, 184 feet; flows at surface; water stands 



WATERS OF THE CRETACEOUS. 221 

4 feet above surface; first water, at 176 feet, stood at —20 inches. Record: 
Soil, 1-10 feet: gravel, 10-40 feet; clay, compact sand. 40-170 feet; sand 
and water, 176-184 feet. 

GRANDVIEW. 

Ray Rushton's well, bored by Sarber in 1904; depth, 183 feet; first water 
at 65 feet, stand —65 feet; second water at 173 feet, stand —150 feet. Re- 
cord: Clay, 0-20 feet; clay and compact sand, 20-173 feet; sand and water, 
173-183 feet. At a depth of 90 feet a stratum of drV. compact sand was 
encountered. 

STATE FARM. 

Well at State farm, S miles northeast of Montgomery, in the N. TC. 
quarter S. W. quarter Section 2, Township 17, Range 18; bored by Gilmer 
& Caylor in 1893; depth, 420 feet; cased to bottom, 4-inch and 6-inch. 

First water at 120 feet, stand —20 feet; 

Second water at 150 feet, stand —16 fefet; 

Third water at 175 feet, stand —6 feet ; 

Fourth water at 200 feet, slight overflow; 

Fifth water at 250 feet, stand, 16 feet above the surface; 

Sixth water at 400 feet, stand 4 feet above surface; flow, 24 gallons per 
minute. Record: Sand and gravel. 0-30 feet; alternate strata of sand 
and gravel and red clay, 30-400 feet; sand and water, 400-420 feet. 

MACON COUNTY 
Surface Features. 

Macon County displays a number of geologic formations in 
its structure, the metamorphic rocks', occupying the northern 
township (18), being overlapped in succession to the south by 
the Tuscaloosa, Eutaw, and Selma chalk, in fairly parallel belts. 
In the southern townships the somewhat irregular bodies of 
the chalk are overlain by the sands, clays, and shell beds of the 
Ripley, over all of which lies the Lafayette capping of red loam 
and pebbles. The Lafayette formation, as usual, affords an 
abundance of good water from springs and shallow wells, and 
the same is true of the Tuscaloosa and to a certain degree of 
the Eutaw. This will explain in some measure the absence of 
artesian borings in these sections. 

Artesian Prospects. 

As far south as Tuskegee the cretaceous beds seem to be 
rather thin and unfavorable for artesian waters, as is shown by 
the uniformly unsuccessful borings at the Tuskegee water- 



222 DETAILS : COASTAL PLAIN DIVISION. 

works, which go into the underlying gneiss. Most of the suc- 
cessful borings, obtaining water in the Eutaw sands', are in the 
region of the chalk, along the Seaboard Air Line, but in no case 
has overflowing water been obtained. 

With the exception of those at Tuskegee and Warriorstancl, 
all the records obtained are of wells along the line of the rail- 
road in the lower part of the county. 

TUSKEGEE. 

City waterworks wells (nine) ; bored by Moore and Mc- 
Creary; depths range from 125 to 180 feet. They supply but 
little water and none of them are now used except in very dry 
seasons', the principal supply coming from a number of springs 
at the foot of a hill just north of the city. Two or three of the 
wells were only 30 to 40 feet deep and overflowed 1 or 2 gal- 
lons per minute. 

WARRIORSTAND. 
Well bored by O. B. Radford; depth, 450 feet; no water in sand. 

CHESSON. 

J. L. Robert's well, bored by O. B. Radford in 1899; depth, 350 feet; 
first water at 325 feet; water stands at —9 feet; steam pump used; pumps 
10 gallons per minute. 

HARDAWAY. 

A. B. Chesson's well, one-half mile southwest of station; bored by O. B. 
Radford- in 1904; aepth, 325 feet; casing, 4-inch; first water at 300 feet; 
water stands at —72 feet. 

Town Well, bored by J. N. Ingram in 1898; depth, 300 feet; casing, 
4 1-2-inch; first water, at 173 feet, stood at —17 feet; second water, at 
300 feet, stood at —20 feet. 

DOWNS AND VICINITY 

W. S. Harris's well, bored by J. N. Ingram in 1902; depth, 356 feet; 
casing, 4 1-2-inch; first water at 325 feet. 

Will Harris's well, one-fourth mile from station; bored by O. B. Rad- 
ford in 1899; depth, 325 feet; first water, at 300 feet, stood at —20 feet. 

James Adams's well, 3 miles north of Downs; bored by O. B. Radford; 
depth, 118 feet; water stands at —25 feet; first water at 118 feet. 

D. Adams's well, 4 miles north of Downs, one-half mile east of Adams 
well; bored by O. B. Radford in 1900; depth, 350 feet; casing, 4-inch; 
first water at 340 feet, stands at —50 feet. 



WATERS OF THE CRETACEOUS. 223 

FORT DAVIS. 

Mrs. Wilson's well, bored by O. B. Radford In 1900; depth, 450 feet; 
casing:, 4-inch; first water, at 425 feet, stood at — 50 feet. 

Karl Russell's well, 7 miles from Fort Davis; bored by O. B. Radford 
in 189S; depth, 218 feet; first water, at 190 feet, stood at —40 feet. 

E. P. Bledsoe's well, Armstrong - , 3 miles east of Fort Davis; bored by 
J. W. Radford in 1897; depth, 450 feet; first water, at 425 feet, stood at 
— 55 feet; steam pump used; pumps 10 gallons per minute. 

ROBA. 

• Clay Crosby's well, bored by Y. T. Radford in 1899; depth, 475 feet; 
casing, 4-inch; first water, at 450 feet, stands at — 60 feet; steam pump 
used; pumps 10 gallons per minute. 



LEE COUNTY. 
Surface Features. 

The surface of Lee County is occupied by the outcrops of 
the crystalline schists and their decomposition products, with 
the exception of a narrow belt at the southern border where 
the sands and clays of the Tuscaloosa overlap the crystalline 
rocks. In the southern half of the county the red loam and peb- 
bles of the Lafayette overlie the older rocks and afford the 
visual conditions for good water from springs' and wells. 

Artesian Prospects. 

The only artesian records in Lee County are from Auburn, 
in the crystalline area, and from Girard, opposite Columbus, 
Ga., in the lower belt, from which it will be seen that the ar- 
tesian prospects are, as a rule, not favorable. 

auburn. 

Alabama Po'ytechnic Institute well, bored by M. F. Fullan in 1899; 
depth, 106 feet; casing, 2-inch; water stood at surface; estimated yield, 
3 gallons per minute with air-lift. Record: Orange sand, 0-10 feet; 
micaceous granite, 10-40 feet; gneissoid granite, 40-45 feet; gneissoid gra- 
nite with comparatively small amount of mica (good water-bearing 
stratum), 45-47 feet; compact gneiss, 47-56 feet; coarse-grained granite, 
small amount of mica, quartz predominating in coarse crystals (good 
water-bearing stratum), 56-60 feet; gneissoid granite, more compact than 
preceding forms and containing iron coloration, 60-106 feet. 



224 details: coastal plain division. 



E. Hill & Co.'s well, bored by J. W. Radford from a depth of 200 feet; 
total depth, 420 feet; casing, 4 1-2-inch and 6-inch; first water, at 360 
feet, stood at — 250 feet. Record: Clay and sand, 200-360 feet; sand 
and water, 36u-390 feet; hard rock, 390-420 feet. This well, beginning in 
the Tuscaloosa beds overlying the gneiss, goes down into the latter at 
390 feet, but the water is obtained from the Tuscaloosa. 



PIKE COUNTY. 
Artesian Prospects. 

An east-west line through Pike County just north of Troy 
would separate the Cretaceous beds' on the north from the 
Tertiary on the south. In the former only the uppermost for- 
mation of the Cretaceous, the Ripley, appears at the surface, 
and in this territory are found practically all the wells whose 
records have been obtained. In all cases it is probable that the 
water is reached in the strata of the Ripley, or "blue marl," as 
it is called. The oldest wells in the county are those about 
Orion, and most of the newer ones are in the same vicinity. 
In parts of this section thick beds of sand, of Lafayette and 
later age, overlie the Cretaceous beds and furnish an ample 
supply of shallow waters, which is probably the cause of the 
dearth of artesian wells'. 

ORION AND VICINITY. 

T. B. Harmon's well, on Gordon place, 2 miles northeast of Orion, in 
the S. W. quarter S. W. quarter Section 29, Township 12, Range 21; flow, 
1 1-2 gallons per minute; water rises to 1 foot above surface; tempera- 
ture 67°. 

Wells on Silver place: No. 1, 2 1-2 miles north of east of Orion, in the 
S. B. quarter N. E. quarter Section 32, Township 12, Range 21; estimated 
flow, 15 to 20 gallons per minute; water rises to 1 foot above floor; tem- 
perature, 66 1-2°. No. 2, 3 miles nearly south of Orion, in the N. E. quar- 
ter Section 4, Township 11, Range 21; inaccessible; in decay, flow decreas- 
ing, probably 1 gallon per minute. 

Well on Oak Grove #lace, owned by Fox Henderson, 1 mile east of Orion, 
near center of Section 6, Township 11, Range 21; flow, 1 gallon per minute; 
water rises to 1 foot above surface; temperature, 68°. 

Well on Jackson place, 4 miles southeast of Orion, in the S. E. quarter 
Section 8, Township 11, Range 21; depth, 332 feet; flow, 40 gallons per 
minute; water rises to 4 feet above the ground; temperature, 69°. 

The wells above mentioned were all put down in 1858 by a well borer- 
named Ledbetter. 

t 



WATERS OF THE CRETACEOUS. 225 

Judge W. R. White's well, :'. 1-1 miles i isl of Orion; bored by J. A. 
Sessions in 1903; depth. 287 feet; diameter, 2 inches; tirst water a1 
feet; second water, .it 270 feet, rose to 6 feet. 

LOGTON. 

Booker Lawson's wells: No. 1, l 1-2 mites west of Logton; bored by 
J. A. Sessions in 1903; depth, 263 feet; first water, at 247 feet, stands at 
—23 feet. No. 2, bored by J. W. Radford in 1901; depth. 304 feet; casing 
i-»nch; tirst water, at 161 feet, stand —30 feet; second water, at 263 feet. 
stand 72 feet. Record: Clay, 0-10 feet; marl. 10-161 feet; sand and water. 
161-187 feet; marl. 187-263 feet; sand and water followed by marl. 263-304 
feet. Mr. Radford did not ease against the first water. He had a sim- 
ilar experience one-half mile south of the above location, the second 
water not rising as high as the tirst. Chunnennugga Ridge is only 
about 6 miles north of Logton and probably 100 feet higher. This ridge 
is the probable source of the first water at Logton, and this may ac- 
count for the exceptional fact that the first water rises 42 feet higher 
than the second water. 

I.I.WVOOD. 

Troy <>il and Chemical's Company's well; bored by J. A. Sessions in 
1903; depth. 80 feet; casing. 4-inch: first water, at 64 feet, stands at —23 
feet; pumps 20,000 gallons per day. 

L. W. Williams's well, 2 1-2 miles east of Linw I; bored by J. A. 

Sessions in 1903; depth, 130 feet; casing. -1-inch: first water, at 1-0 feet, 
stands at —83 feet. Record: Sand. 0-4 feet; (?), 4-14 feet; marl. 14-12.) 
feet: sand and water. 120.-130 teet. 

( hilv one attempt at an artesian well in the Tertiary area 
of Pike County, -viz, at Troy, the county seat. This well is 
on a moderately high ridge similar to Chunnennugga Ridge in 
Bullock Comity. The lower part of Pike Comity is. in genera! 
well watered, the materials of the Tertian- formations, like 
those of the overlying Lafayette, being suited to the absorption 
and storage of the rainfall. The Clayton member of the Ter- 
tiary does not differ widely in its materials from the Ripley 
underlying it, so that it is not easy to draw the line between 
Cretaceous and Tertiary in the Troy record. 

The Xanafalia sands occupy the surface in the lower town- 
ships of the county, and there should be no difficulty in getting 
artesian waters from them. 



Public well, bored at the expense of the city; elevation, 581 feet; depth. 
2,ii32 feet; How of about 75 gallons per minute obtained at depth of 450 
feet, hut. lost when the well was lowered; well finally abandoned after 

boring cost about $26. 

15 



226 details: coastal plain division. 

The following record was made by the borer, Mr. Conover, and 
at the Troy Normal College together with a drawing of the well. 

Record of public well, Troy. 



Feet. 

Clay — 12 

Yellow sand 12 — 120 

Shell rock 120 — 126 

Green marl 126 — 186 

Shell rock 186— 190 

Quicksand 190 — 80S 

Compact sand 30S — 753 

Quicksand 753 . . 792'. 

Compact sand 792 — 79S 

Coarse white sand and water 798 — 914 

Blue sand 914 — 954 

Blue marl 954 — 1598 

Compact sand 1598 — 1606 

Green marl 1606 — 1614 

Shell rock and coral 1614 — 1622 

Compact sand 1622 — 1642 

Blue marl 1642 — 1762 

Coarse sand 1762 — 1770 

Coal (lignite) 1770 — 1770 % 

. Green marl and sand 1770 y 2 — 1780 % 

Compact sand; coal (lignite) 2 inches.. 1780 y 2 — 1784 y 2 

Coal (lignite) 1784 y 2 — 1785 y 2 

Blue marl 1785 y 2 — 2585 V 2 

Compact sand 2585 V 2 — 2605 % 

Gray marl 2605 y 2 — 2632 % 



At this depth the boring should almost reach the crystalline rocks after 
passing through the entire thickness of the Cretaceous formations. The 
uncertainty as to what is meant by the word marl makes it impossi- 
ble to determine accurately the formation in which the boring stopped. 



BULLOCK COUNTY. 

Surface Features. 

The most marked topographic feature of Bullock County is 
the Chunnennugga Ridge, which makes the divide between the 
waters flowing northward into the Alabama and those flow- 
ing southward into Chattahoochee, Pea, and Conecuh rivers. 
Like all s'uch ridges (called "cuesias" by geographers) in the 
Coastal Plain, Chunnennugga Ridge has a steep infacing 
(northward) slope and a very gentle, in places hardly percep- 
tible slope in the other direction. In most parts of the county 
the northern edge of this ridge marks approximately the line 
of contact between the Selma chalk and the sandier strata of 
the Ripley. 



WATERS OF THE CRETACEOUS. 227 

Aetesian Prospects. 

In the northern or limestone half of the county artesian wells 
are the main source of water, which is derived from borings 
varying- in depth with the location. The record given below of 
the Gray well at Mitchell Station (altitude 252 feet), on the 
Central of Georgia Railway, is interpreted as indicating that 
the boring goes through the Selma chalk and into the Eutaw 
sands below. The designations marl, rotten stone, etc., in this 
record are not easy to interpret, but the location of Mitchell 
station is such as to make the thickness of the chalk there 
about 200 feet or less. 

MITCHELL STATION. 

Eli Gray's well, bored by Frank Tillotson; depth. 394 feet; casing 
enlarged from 3 1-2-inch to 6-inch on account of sand; cased to marl. 
Record: Top soil, 0-18 feet; marl, 1S-26S feet; limestone, 268-269; rotten 
stone, 269-319 feet; marl, 319-394 feet. 

Frank Rutland's well, bored by Y. T. Radford in 1899; depth, 380 feet; 
casing, 4-inch; first water, at 350 feet, stood at —20 feet. 

FITZPATRICK. 

Atlantic Compress Company's well, bored by Y. T. Radford in 1903; 
depth, 450 feet; casing, 4-inch; first water at 400 feet; water stands at 
— 20 feet; steam pump gives 20 gallons per minute. 

THOMPSON STATION. 

Dallas Patterson's well, bored by O. B. Radford in 1897; depth, 540 feet; 
casing, 4-inch; first water, at 520 feet, stood at —39 feet. 

NORTH OF CHUNNENNUGGA RIDGE. 

Other records of borings in the limestone country north of Chunnen- 
nugga Ridge are as follows: 

Bob Gholson's well, 2 1-2 miles southwest of Fitzpatrick; bored by J. W. 
Radford in 1900; depth, 535 feet; casing, 4-inch; first water, at 500 feet, 
stands at — 45 feet. 

A. V. Barnett's well. High Log post-office, 5 miles southwest of Fitz- 
patrick; bored by Y. T. Radford in 1S98; depth, 700 feet; casing, 4-incii; 
first water, at 680 feet, stood at —60 feet; pumps 10 gallons per minute. 

SHOPTON, AND VICINITY. 

Gus Edwards's well, bored by J. W. Radford in 1901; depth, 1050 feet; 
casing, 4-inch; first water, at 1000 feet, stands at —150 feet; yield, 10 gal- 
lons per minute with steam pump. 



228 details: coastal plain division. 

George Edwards's well, ' 2 miles east of Shopton; bored by Sessions 
in 1901; depth, 9SS feet; casing, 4-inch; first water, at 988 feet, stood at 
—200 feet. 

BUGHALL. 

E. C. Dawson's well, bored by O. B. Bradword in 1898; depth, 1000 feet; 
casing - , 4-inch; stoppea in marl; no water. 

UNION SPRINGS AND VICINITY. 

Singleton & Linton's well, 4 miles northwest of Union Springs; bored by 
J. W. Radford in 1899; deptn, 666 feet; casing, 4-incn; first water at aGO 
feet; second water at 636 feet; third water, at 65t> feet, stands at — 122 
feet. Record: Soil and clay, 0-45 feet; marl, 46-560 feet; sand and water, 
560-620 feet; flint rock, 620-636 feet; sand and water, 636-641 feet; flint 
rock, 641-655 feet; sand and water, 655-666 feet. 

A. E. Singleton's well, 3 1-2 miles west of Union Springs; bored by J. VV. 
Radford in 1900; depth, 650 feet; casing, 4-inch; first water, at 600 feet, 
stood at — 125 feet. 

S. P. Rainer's well, 1 mile west of Union Springs; bored by Y. T. Rad- 
for~ in 1899; depth, 815 feet; casing, 4-inch; first water, at 775 feet, 
stood at — 160 feet. 

Well of j. H. Rainer, Jr., 3 1-2 miles north of Union Springs; bored by 
Y. T. Radford in 1901; depth, 610 feet; casing, 4-inch; first water, at 590 
feet, stood at — 120 fee.. 



Union Springs is on the summit of Cunnennugga Ridge, 
which, as before stated, is on the contact of the Selma chalk 
with the Ripley sands and clays. The altitude of the ridg-; 
here is between 485 and 515 feet, and borings for water are 
necessarily deep, and with no prospect of flow. The wells 
which supply the city show that the water stands at — 238.5 
feet, from which depth it is' pumped by air lift. The record is 
as follows : 

City waterworks wells, Union Springs; altitude, 519 feet; two wells, 
same record for both; bored by D. A. Caylor, and record furnished by 
him; commenced in 1894, completed in 1S95; depth, S4S 1-2 feet; cased 
to the bottom with 8-inch casing; rests on very hard impenetrable rock; 
water stands at 238 1-2 feet; pumps 140 gallons per minute; temperature, 



Record of city ivaterworks wells, Union Springs. 



Feet. 

Top soil — 16 

Marl, with seams of light-gray rock, vary- 
ing in thickness from 2 to 12 inches 
occurring every 25 feet 16 — 84S V 2 



WATERS OF THE CRETACEOUS. 229 

Analysis of xcater from city waterworks wells. Union Springs. 
(Analyst, /.'. S. Hodges.) 

Parts per million. 

Potassium (K) 6.6 

Sodium (Na) 61.4 

Magnesium (Mg) 

Calcium (Ca) 2.5 

Iron and alumina (FeoO :! Al-.O.-,) .7 

Chlorine (CI) 9.4 

Sulphuric acid (S0 4 ) 31.8 

Carbonic acid (HCO s ) 124.8 

Silica (Si0 2 ) 15.1 

252.5 
EAST OF UNION SPRINGS. 

Eastward from Union Springs the Ridge loses its distinctive 
character, passing gradually into the high dividing line between 
the Alabama and Chattahoochee drainages. The two records 
which follow come from this high land. The waters from the 
.wells in this section, in both Macon and Bullock counties, are 
said to have a strong odor of sulphur. 

Atlantic Compress Company's well. Suspension: bored by Y. T. Rad- 
ford in 190o; depth. 700 feet; casing, 4-inch; first water, at 700 feet, stood 
at —140 feet. This well caved, but another a short distance away gave 
4 1-2 gallons pm- minute with pump. 

J. Bank's well, Guerrytown; bored by O. B. Radford in 1904; depth. 600 
feet; casing. 4-inch; first water, at 5b0 feet, stood at — 7 feet. As soon 
as pump is used, water falls to — 100 feet. 

SOUTH OF UNION SPRINGS. 

South of Union Springs deep beds of sand, either of Lafay- 
ette or more recent formation, overlie the Ripley strata, the 
characteristic red loam and pebble beds of the Lafayette, how- 
ever, appearing in many localities. This part of the county is 
consequently well supplied with shallow waters and deep bor- 
ings are rare. Only the two following records could be ob- 
tained : 



J. C. Graham's well, Inverness; bored by Y. T. Radford in 1902: depth, 
925 feet; casing. 4-inch: no water. Record: Quicksand. 0-10 feet; marl, 
10-300 feet; sand, dry. 300-315 feet; marl. 315-925 feet; stopped in marl. 

W. S. Deason's well, near Eric; bored by Sessions in 1903; depth. 106 
feet; diameter, 4 inches: first water, at 106 feet, stands at -45 feet. 



230 details: coastal plain division. 

chattahoochee river drainage. "blue marl" region, 
stratigraphic characters. 

East of Macon County the three upper divisions of the 
Cretaceous, so easily distinguished to the west, can not be made 
out with any definiteness. The succession and character of the 
strata along Chattahoochee River are somewhat as follows : 

First. A great series of bluish micaceous and clayey sands', 
with indurated ledges, all more or less fossiliferous ; and mas- 
sive bluish clays, sometimes with lignitic matter, along Chatta- 
hoochee River for a distance of 35 or 40 miles', corresponding 
to a thickness of 1000 feet or more. These beds, or at least 
the upper half of them, contain shells characteristic of the Rip- 
ley formation. 

Second. A series of cross-bedded sands, with clay partings, 
the latter, when thick, containing many fragments of ligni- 
tized stems and leaves' and occasionally large logs, also ligni- 
tized ; dark-colored rhicaceous sands with indurated ledges in 
which are fossil oysters ; nearly black, somewhat sandy clays 
and clayey sands, with many fossils, mainly in the form of 
casts'. These beds have a thickness of about 400 feet along the 
river. The fossils of this series, so far as they have any dis- 
tinctive characters, seem to be closely related to the species 
occurring in the upper part of the Eutaw sands. 

Third. The cross-bedded sands mottled clays, gray clays, 
and other characteristic materials of the Tuscaloosa formation, 
extending from Broken Arrow Bend, 8 miles below the city 
up to Columbus, Ga., and perhaps farther. This formation 
seems to be much thinner in the eastern part of the State than 
farther west. 

It will be seen that the Selma chalk as a distinct division, 
recognizable by its physical characters and its fossils, has given 
out, strata with Eutaw fossils being directly overlain by strata 
with fossils characteristic of the Ripley, into which the chalk 
has apparently merged. In Russell and Barbour counties the 
Ripley beds, which occupy a large proportion of the surface 
have the general designation of "blue marl." 

Along the upper border of Russell County the Tuscaloosa 
beds are exposed about Columbus, Ga.. and Girard and on tht 
river bluffs from Columbus down to Broken Arrow Bend, where 



WATERS OF THE CRETACEOUS. 231 

the dark-gray calcareous sands with fossils of the lowermost 
Eutaw arc encountered. The other strata of the Eutaw, con- 
sisting of clave) sands, laminated dark-gray clays', and yellow 
and white sands, are exposed along the river bluffs from Bro- 
ken Arrow Bend to the mouth of Ihagee Creek. 

From Ihagee Creek down to Otho, below Eufaula, the river 
banks show the succession of the Cretaceous beds, which are 
extremely uniform in lithologic character and which contain 
throughout the characteristic fossils of the Ripley group, often 
in the finest state of preservation and of such fresh appearance 
as to suggest, at least, that they are of Tertiary age. These 
beds, known throughout this part of the State as "blue marl", 
consist of bluish or gray calcareous effervescent sands, gener- 
ally containing either shell fragments or entire shells, scales 
of mica, grains of glauconite, bits of lignitic matter, etc. The 
sands show variations in the proportion of clay, mica, and lig- 
nitic matter, and also in the color, which shades out to yellow 
where much weathered and merges into brown where the pro- 
portion of iron is considerable and the material is not too 
much exposed and dried out. Some shade of blue or dark 
gray is in the main, characteristic of the whole series below the 
level of ground water, and this justifies the name of blue marl, 
if the word marl be used to designate beds of almost any ma- 
terial containing shells or fragments of shells. The bluish 
s'andy beds alternate at frequent intervals with indurated ledges 
of similar materials compacted into rather hard rocks by a cal- 
careous cement. Such ledges usually contain large numbers 
of the shells of the various oysters characteristic of the Creta- 
ceous, such as Bxogyra, Grypliaca, Anomia, Ostrea in several 
species. 

From this account it would seem that the Eutaw and Ripley 
beds in this section afford fairly good conditions for artesiat; 
water and the records which have been obtained appear to in- 
dicate that both formations do yield such water: flowing wells 
are, however, rare. 

Russell and Barbour are the two typical "blue-marl" counties, 
but many of the characteristics of this region are observed in 
the Cretaceous' formations of Pike County and of the southern 
part of Bullock County, and the artesian conditions of these 
sections are practically the same as those described in Russ-.d! 
and Barbour. 



232 details: coastal plain division, 

county details. 

RUSSELL COUNTY. 
Surface Features. 

The topography of Russell County does not offer any very 
marked peculiarities. As usual, many of the high divides are 
capped with the Lafayette mantle of red loam and pebble.- 
making level plains in which an abundance of good water can 
always be had from wells and springs. In the blue marl region, 
where the Cretaceous beds are not covered by this mantle of 
Lafayette, water may generally be had in wells varying in 
depth from 30 feet in the lowlands to 50 or 60 feet in the up- 
lands. If it is not obtained at that depth, it will not be found 
by penetrating info the blue marl. Some of these wells go dry 
in summer, and especially was this the case in 1897. 

The records given below are instructive. It is to be remarked 
that the water in these borings stanch; at a higher level than is 
generally the case. In most of the State the water does not 
overflow when the altitude of the well is much above 225 feet, 
and not always at lower elevations. At Hurtsboro, with an 
altitude of 346 feet, the water stands within a few feet of the 
surface (8 or less), as it does also at Hatchechubbee, with an 
altitude of 311 feet. 

Artesian Records. 

kaolin station. 

Two wells, bored by the City of Columbus, Ga., one mile 
south of the City, near Kaolin Station on Central of Georgia- 
railway. 

No. 1 drilled by L. B. Clay, of Bartow, Ga., Depth 286 feet 
diameter not known ; water rises 12 to 15 feet above the ground. 
Record — Clay, etc., 0-5 feet; sand and gravel, 5-33 feet; decom- 
posed sand rock, gravel and chalk, 33-53 feet; hard chalk, marl 
and soft rock, 53-113 feet; water bearing strata, 113-116 feet; 
marl, 1 16-146 feet; water bearing strata, 146-153 feet; marl and 
rock, 153-173 feet; artesian water strata, 173-185 feet; red 
clay, blue marl and soft sand rock, 185-235 feet; hard rock, 
235-238 feet; water sand, or honey comb water bearing rock. 



WATERS OF TIN; CRETACEOUS. 233 

238-245 feet; Mint rock, very hard. 245-246 feet; alternating 
thin layers oi marl ruck and water bearing strata. 2.40-2X1 feet; 
granite rock, very hard 281-280 feet. 

No. 2. Drilled by Perry Andrews of Atlanta, ('.a., Depth 
about 280 feet; diameter 12 inches; estimated flow 5.000 gal- 
lons a day without pumping, estimated yield by air lift 120,000 
gallons a day. Water rises 12 to 15 feet above the surface 

In both these wells the underlying granite was reached and 
the boring discontinued at about 280 feet depth. 

HURTSBORO AMI VIC! MTV. 

Public well. Hurtsboro; altitude. 340 feet; bored in 1?9S by Morrison and 
Wicker; top soil. 15 feet; sand and marl. 110 feet; two ledges of shell 
rock in the marl. 2 feet; compact sand and shell rock every 3 or 4 feel 
down to 400 feet; water-bearing sand witli some red clay at bottom; total 
depth. 530 reet; casing, 50 feet. 4-inch; water stands at -9 feet; tempera- 
ture 6S°. 

W. H. Rank's well. Hurtsboro; depth. 520 feet; water stands at -8 feet; 
temperature, 00°. Record: Top to blue marl. 08 feet; marl. 125-200 feet 
thick, with about 20 ledges of shell rock, very hard; compact white 
sand between the ledges of shell rock; hard red clay under the marl; 
then water-bearing sand. 

J. P. Crawford's well. Hurtsboro; bored in 1?9S; depth, 302 feet; casing. 
102 feet, 2%-inch; water stands at -2% feet; pump easily exhausts flow; 
flows freely after five minutes; water colors vessels. 

Record of ■!. P. Crawford's well, Hurtsboro. 



Feet. 

Rime rock — 12 

Shell rock 12 - 13% 

Grav and red sands 13% — S5 

Marl 85 — 107 

Grav flint rock 107 1 1 8 

Hard marl 108 —138 

Rock 138 139 

Marl 139 — 185 

Rock 185 —187 

Marl 187 — 200 

Gray sand 200 —215 

Hard rock (water rose to -4% feet) 215 — 217 

Sand and mica 217 — 243% 

Rock 243% - 2 1 1 

Compact sand 244 — 240 

Sand and mica 240 —263 

Sand and lignite 203 — 278 

Water-bearing sands 2'n, —302 



Eton Tucker's well, Hurtsboro, one-fourth mile northeast of Craw- 
ford well; bored by Mr. Tucker in 1902; depth. 500 feet; water stands at 
-24 feet; record same as other Hurtsboro wells. 



234 DETAILS : COASTAL PLAIN DIVISION. 

HATCHECHUBBEE AND VICINITY. 

C. E. Ingram's well, Hatchechubbee; altitude, 311 feet; depth, 400 feet; 
water stands at surface; casing, 20 feet, 3-inch. 

Record of C. E. Ingram's well, Matchechubbee. 



Feet. 

Top Soil — 20 

Marl 20 — 100 

Coarse sand, with shell rock 100 — 140 

Hard greenish marl l-±0 — 200 

Sand and shell rock 200 — 300 

Pink marl . 300 — 350 

Red clay (bottom sand) 350 — 400 



The wells of L. C. Cooper, F. P. Pladdock, J. M. DeLacy, and A. B. 
Walker, in Hatchechubbee, were all put down at the same time; all are 
close together and the records are the same as that of the Ingram well. 

McMicken well, 3 miles south of Hatchechubbee; bored by W. M. Mor- 
rison in 1898; water stands at -50 feet; casing, 20 feet, 3-inch; top to 
marl, 12 feet; marl 130 feet thick; thin ledge of shell rock. 

Jim Perry's well, 8 miles south of Hatchechubbee; record same as that 
of McMicken well. ' 

SEALE AND VICINITY. 

Court-house well, Seale; bored in 1898 by Wicker & Morrison; depth, 
170 feet; water stands at -30 feet; casing, 120 feet, 3-inch; 90 feet through 
clay, coarse gravel, and coarse sand with small black grains; this sand 
alternates with shell rock from 6 inches to 2 feet in thickness; log at 40 
feet. 

J. S. Brannon's well. 2% miles north of Seale; depth, 400 feet; water 
rises to -75 efet; casing, entire depth, 4-inch. 

OSWICHEE. 

W. J. McLendon's well, near Chattahoochee River; depth, 465 feet. Rec- 
ord: Sand and clay, 20 feet; marl with shell, 65 feet; beds of sand and 
marl, 15 to 25 feet thick, alternating, to 380 feet; hard rock, 2 feet; sand 
to 445 feet. Water at this point flowed 12 gallons per minute, but has de 
creased to 4 gallons. Well lowered 20 feet into sand to hard rock. 



WATERS OF Till-; CRETACEOUS. 235 

Analysis of water from W ■/. McLendon's well, Oswicliee. 
i I nalyst, /«'. .v. limine*, i 



Parts per million. 

Potassium (K) l.S 

Sodium (Na) 23.9 

Magnesium (Mg) .7 

Calcium (Ca) 11.5 

Iron and alumina (Fe 2 3 . Al->0 3 ) 2.0 

Chlorine (CI) 1.7 

Sulphuric acid (S0 4 ) fi.4 

Carbonic acid (HCO ;l > 93.5 

Silica (SiO = ) 36.8 

178.3 



Of the wells described above, those at Oswichee and Seale 
undoubtedly go into the Eutaw formation, since these two 
places are close to the contact of the two formations. The wells 
at Hatchechubbee also penetrate into the Eutaw, but the two 
south of Hatchechubbee barely reach it. The deepest of the 
Hurtsboro wells may go down to the Eutaw, but the shallower 
ones' hardly do so. 

The wells along the Seabord Air Line, described below, are 
farther from the contact of the Eutaw and Ripley, and as they 
are relatively shallow they do not pass out of the Ripley sands 
or marls. 

Rl'THERFOKD AND VICINITY. 

R. P. Tallman's well. Rutherford, 10 miles southeast of Hurtsboro; bored 
by W. E. Wicker in April. 1S9S; depth, 1G4 feet; casing. 22 feet, 3-inch; 
flow. 18 gallons per minute; piped into residence; temperature. 68°. Rec- 
ord: Top to marl, 22 feet: marl with ledges of shell rock, 100 x'eet. Later 
information is that the water here has ceased to flow and that other 
wells in the vicinity of Rutherford and Hurtsboro either no longer flow 
or have much weaker streams than when first bored. 

H. M. Rutherford's well. Rutherford; depth. 135 feet; casing, 20 feet, 
3-inch; flowed 6 gallons per minute for two years, stands now at surface; 
temperature, 68°. Record: Top soil. 18 feet; marl, about 100 feet; bal- 
ance sand and water. 

Mr. W. M. Morrison bored two more wells for Mr. Rutherford in 1901 
and furnishes the following details: No. 1. at residence; depth, about 
180 feet; water stands at -1 foot. Record: Clay and sand, 20 feet; blue 
marl. 130 feet; hard shell rock. 6 inches; water-bearing sand. 30-40 feet; 
hard blue rock. 4 feet; sand to bottom. No. 2, at store, near railroad; 
same depth and record as No. 1; flow. iy 2 gallons per minute. 

G. L. Hardin's wells, Rutherford: No. 1. "brick-yard well," three- 
fourths mile south of Rutherford; bored by Mr. Hardin in 1902; depth. 105 
feet; casing, 3-inch; first water, at 90 feet, stood at 6 feet above the sur- 



236 details: coastal plain division. 

face; flow, weak; present flow, 3 gallons per minute; water rises to 3 
feet above the surface; temperature, 66°. Record: Soil, 0-15 feet, at 60 
feet. 18 inches of soft shell rock; sand, 90-105 feet. No. 2, "ginnery well," 
one-half mile east of Rutherford; bored by Mr. Hardin in 1899; depth, 
140 feet; casing, 3-inch; first water, at 120 feet, stood at 18 feet above 
the surface; flow, 3 gallons per minute; temperature. 66°. No. 3, three- 
fourths mile west of Rutherford; bored by Mr. Hardin in 1901; depth, 130 
feet; casing, 3-inch; first water at 115 feet, stood at 1 foot above the sur- 
face; flow 2 gallons per minute; temperature, 66°. Record same as oth- 
ers. 

N. W. B. Long's well, 1 mile northeast of Rutherford; depth, 120 feet; 
water stood at -4 feet; increased to small flow; gravel, marl, and sand. 

Well on Hatcher plantation, iy 2 miles northwest of Rutherford; depth, 
160 feet; flow, 5 gallons per minute; cased to marl with 3-inch casing. 

T. L. McDonald's well, 2 miles northwest of Rutherford; bored by G. L. 
Hardin in 1900; depth, 260 feet; first water stands at -60 feet. 

Well on plantation of S. T. Margaret, 2 miles south of Rutherford; 
'bored by W. M. Morrison in 1901; flow, 1 gallon per minute. Record: 
Clay and sand. 15 feet; blue marl to 130 feet; gray sand and water to 175 
feet. 

Gus Battle's well, 2 miles south of Rutherford, on high red hill; bored 
by W. L. Morrison in 1901; water stands at -40 feet. Record: Clay and 
sand, 70 feet; blue marl to 210 feet; water-bearing sand, 30 feet. 

Upshaw Brothers' well, 3% miles southeast of Rutherford; bored by 
Geo. Thompson in 1901; depth, 150 feet (?); flow, 3 gallons per minute; 
water rises to 2 feet above the surface; temperature, 67°. 

Mr. Thompson also bored two wells at Persons Crossing, 3 or 4 miles 
east of Rutherford, about which no reliable information could be ob- 
tained. One is owned by J. W. Upshaw and the other by T. L. Mitchell. 

PITTSBORO AND VICINITY. 

Well at store of J. W. Upshaw, near Hooks Station, 8 miles west of 
Pittsboro; bored by Wicker in 1898; depth, 325 feet; water used is from 
strata at 122 feet; water rises to -35 feet; unlimited supply; colors ves- 
sels; casing. 20 feet, 3-inch. Record: Top soil, 0-20 feet; marl with 
ledges of shell rock, 20-120 feet; sand and water. 120-122 feet; marl, 122- 
325 feet. 

Well on L. C. Lamb's plantation. S miles west of Pittsboro; bored in 
May, 1898; depth, 129 feet; casing, 24 feet. 3-inch; flow, 10 gallons per 
minute; temperature, 67°; colors Vessels. Record: Top soil, 0-20 feet; 
marl, 20-128 feet; shell rock, sand underneath, 128-129 feet. 

Well at R. B. Adams's plantation, ZV 2 miles northwest of Pittsboro; 
bored by Wicker in 1898; casing, 20 feet 4-inch; water rises to -50 feet; 
very hard; pumps free, supply inexhaustible. Record: Top to marl, 
18 feet; water and sand; 97 feet; does not go below the marl. 

Well at L. C. Lamb's residence, V/ 2 miles northwest of Pittsboro; bored 
by Wicker in 1898; casing, 20 feet, 4-inch. Record: Top to marl, 18 feet; 
bored to 97 feet to sand and water, marl underneath. 

Public well, Pittsboro; bored by W. E. Wicker in 1898; casing, 26 feet, 
3-inch; flow, three-fourths gallons per minute; temperature, 72°; tastes 
of sulphur and colors vessels with iron; stated to be good for stomach 
troubles. Record: Surface to marl, 24 feet; marl, with two layers of 
hard shell rock, 193 feet; quicksand, 2 feet, with hard rock at bottom. 
The analysis of the water from this well by Mr. Hodges, is as follows: 



WATERS OF THE CRETACEOUS. 237 

Analysis of water from public well, Pittsboro. 



Parts per million. 

Potassium (K) 1.5 

Sodium (Na) 59.1 

Magnesium i Mgi .8 

Calcium (Ca) 9.0 

Iron and alumina ( FV..( >.,. A1..0 S ) .9 

Chlorine (CI) 61.3 

Sulphuric acid (SO.,) 1.6 

Carbonic acid (HCO a ) 82.6 

Silica (Si0 2 ) 41.0 

257.8 



Well at J. \Y. Caldwell's gin. Pittsboro; depth, 445 feet; casing, 26 feet, 
3-inch; original flow, one-half gallon per minute; present flow, 1 quart 
per minute; temperature, 72°; colors vessels. 



ttecord of J. W. Caldwell's well, Pittsboro. 



Feet. 

Top si.il — IS 

Marl IS — 78 

Shell rock 78 — 78% 

Marl, sand and water (1 gallon in 8 minutes). 7S 1 / £ — 225 
Marl, sand and water (% gallon per minute). 225 — 205 
Marl (hard rock at bottom; 265 —445 



F. P. Pitts's well, at residence. Pittsboro; depth. 217 feet; temperature, 



Record of /'. P. Pitt's well, Pittsboro. 



Feet. 

Top Soil 0— 20 

Marl 20 — 60 

Soft shell rock 60 — 61 

Marl 61 — 75 

Sand 75 — 80 

Hart flint rock 80 — 82 

Marl (water and sand. 1 quart in 12 minutes).. 82 — 165 

Marl 165 — 185 

Marl (flow increased to 32 gallons per minute. 

drill lost) 185 — 217 



OLENVIIXE AND VICINITY. 

Comer-Bishop Company's well, on Cowikee Creek, near Glenville; bored 
by Morrison in 1899; depth. 514 feet: water stands at -9 feet. Record: 
Clay, 0-8 feet; coarse gravel, 8-18 feet; marl, shell rock, 4 inches thick, 
18-294 feet; water-bearing sands. 294-514 feet. 



238 DETAILS : COASTAL PLAIN DIVISION. 

Wells on on Capt. B. C. Perry's plantation, near Glenville: ■No. 1, 
depth, 164% feet; casing, 22 feet, 3-inch; water rises to 25 feet above the 
surface; flow, 100 gallons per minute; temperature, 67°. 

Record of E. G. Perry's well, No. 1, near Glenville. 



Feet. 

Top soil — 15 

Quicksand 15 — 17 

Marl 17 — 160 

Shell rock 160 —160% 

Water-bearing sands 160% — 164% 



Analysis of water from, E. C. Perry's tcell No. 1, near Glenville. 
{Analyst, R. 8. Hodges.) 



Parts per million. 

Potassium (K) 8.6 

Sodium (N-a) 87.2 

Magnesium (Mg) 1.5 

Calcium (Ca) 36.5 

Iron and alumina (Pe 2 3 , A1 2 3 ) 1.8 

Chlorine (CI) 73.5 

Sulphuric acid (S0 4 ) 175.9 

Carbonic acid (HCO a ) 12.8 

Silica (Si0 2 ) 19.4 

417.2 



No. 2, one-half mile from No. 1; bored by Geo. Thompson in 1899; depth, 
175 feet; flow, 60 gallons per minute; temperature, 67°. Record same as 
No. 1. 

Wells on Hatcher's plantation, on Chattahoochee River; 4 or 5 flowing 
wells are reported here, but no records were obtainable. 



BARBOUR COUNTY. 

Surface Features. 

The area of Barbour County is about equally divided between 
the Ripley division of the Cretaceous on the north and the 
lower divisions of the Tertiary on the south. 

Some details have already been given under Russell County, 
of the Ripley strata as exhibited in the eastern counties of this 
section. These beds consist in the main of bluish or grayis'h' 
sands, with scales of mica, grains of greensand, and very gen- 
erally fragments and decomposed masses' of marine shells. 



WATERS OF THE CRETACEOUS. 239 

The presence of calcareous material in the sands has caused 
the name marl to be applied to them and to the formation as a 
whole throughout this part of the State. Besides the sandv 
marl, thick beds of somewhat massive clay are not uncommon 
in some parts of the comity, where they form the basis of a 
certain class of soils known as the "hog wallow" prairie. 

South of the latitude of Clayton the Tertiary strata lap over 
those of the Cretaceous and determine in great measure the 
character of the soils and of the topography. The contact of 
Cretaceous and Tertiary in many parts of this county is' marked 
by a well-defined ridge similar to the Chunnennugga Ridge of 
Bnllock County, though differing in the geologic formations in- 
volved. 

In its upper part this ridge, which may be called the Clay- 
ton Ridge, is made by the Clayton limestone, with a double 
capping consisting of beds of the Grand Gulf massive and 
laminated clays and sands, and the usual red loam, sands, and 
pebble beds of the Lafayette. 

The northward-facing slope of Clayton Ridge is steep and 
well marked, while the southward slope, being structural, is 
gentle and scarcely to be distinguished from a level plain. On 
the summit of the ridge is the town of Clayton, to the north of 
which lie the calcareous lands of the "blue marl" region, while 
to the south the surface is generally sandy, partly from the 
materials afforded by the Tertiary strata and partly from the 
overlying Grand Gulf and Lafayette deposits'. 

The presence beneath the surface of limestone of the Clay- 
ton and Nanafalia horizon is shown for many miles south of 
its outcrop by the bold springs of blue limestone water which 
break out in places in the lower part of the county. The be^t 
known of these is the Blue Spring, a place of resort for people 
from all parts of the count}'. This' spring breaks out in the 
bottom of Choctawhatchee River and occupies a nearly circular 
area about 25 feet in diameter. The water is clear and blue 
like that of the Big Springs of Florida, but of considerably 
lower temperature. 

In both Cretaceous and Tertiary terranes the divides are 
often high, level plains capped with the materials of the La- 
fayette. As a matter of course surface waters in such regions 
are abundant and of good quality. In the Tertiarv formations 



240 details: coastal plain division. 

also there seems' to be no lack of water supply from ordinary 
wells and springs. 

In the northern half of the county, on the other hand, where 
the Lafayette sands are not present and the water must be ob- 
tained from the blue marl strata, the supply is deficient and ar- 
tesian borings are necessary. 

Artesian Prospects. 

The few available records of the bored wells of Barbour 
show that the borings have not gone deeper than the Riplej 
strata, except possiblv in the case of the Eufaula Oil and Gin 
Company's well which may have reached the Eutaw sands. It 
may be remarked again in this connection- that along Chatta- 
hoochee River below Columbus', the whole Cretaceous series 
above the Tuscaloosa, shows a great uniformity of material, 
so that it is not easy to distinguish between the Eutaw and the 
Ripley where there are no fossils available. 

EUFAULA AND VICINITY. 

At Eufaula the altitude of the well from which the city 
supply is derived is no feet below that of the railroad track 
at the depot, or 90 feet above mean tide ; that of the Oil and 
Gin Company's well is about the same as that of the depot-200 
feet above tide; and that of the well at Moulthrop's brick yard 
is probably intermediate between the two. At the two lower 
wells the water overflows, but not at the other. In all these 
the supply seems to be inadequate. 

City Water Company's well,' Eufaula. under the bluff on the west 
bank of Chattahoochee River, 110 feet below the city; casing, 4-inch; flow, 
5 3-4 gallons per minute; hydraulic ram used; temperature, 68°. Boring 
is in marl to water-bearing sands at 4C0 feet; several layers of soft rock; 
hard rock below the water-bearing sand. 

Eufaula Oil and Gin Company's well. Eufaula; bored in 1895; depth, 950 
feet; water at first stood at -26 feet; now stands at -50 feet; cased at 300 
feet. 4-inch and 6-inch; supply insufficient; well abandoned. 



WATERS Of THE CRETACEOUS. 241 

Record of Eufaula Oil and Gin Company's well, Eufaula. 



Feet. 

Top soil and sand 0— 30 

Marl 30 — 380 

Soft sandstone ., 380 — 381 

Cavity with a little water 381 — 389 

Marl, water below in very fine sand 389 — 950 



Well at Moulthrop's brick yard. 1 mile southeast of Kufaula; bored 
in April. 1900. by Eugene Thompson; depth. 350 feet; casing, 20 feet, 
4-inch; flow, 5 gallons per minute. Record: Top soil, 0-20; marl water, 
20-350. The water bearing bed in this well is a sharp gray sand of fine 
grain, used by engineers for grinding valves. The boring went 15 feet 
deeper than this sand and struck a hard rock which was not pierced. 
The marl contains a great many shells, and in it at intervals of about 
30 feet occur indurated crusts. The following analysis of the water from 
this well was made by the Pratt Laboratory, of Atlanta, Ga. 

A?ialysis of water from Moulthrop's well, Eufaula* 



Parts per million. 

Sodium (Na) 136.92 

Potassium (K) 3.05 

Calcium (Ca) 3.49 

Magnesium (Mg) .79 

Chlorine (CI) 13.68 

Sulphuric acid (S0 4 ) 5.25 

Carbonic acid (CO<0 172.83 

Iron and alumina (Fe 2 3 , AUO3) 1.88 

Silica (Si0 2 ) 15.92 

Organic and volatile matter 33.02 

386.83 



*Expressed by analyst in grains per gallon and hpothetical combi- 
nations ; recomputed to ionic form and parts per million at U. S. 
Geological Survey. 

Comer-Bishop Company's well, on Jennings Fryer place, 6 miles north 
of Clayton; bored by W. L. Morrison; record furnished by him; depth, 
277 feet; water stands at —80 feet. Record: Top soil, 0-30 feet; marl, 30-120 
feet; sand with layers of very hard rock, from 4 inches to 4 feet thick, 
120-277 feet. The analysis of this water, by Mr. Hodges, is as follows: 



16 



242 DETAILS : COASTAL PLAIN DIVISION. 

Analysis of water from Comer-Bishop Company's icell, near Clayton, 



Parts per million. 

Potassium (K) 3.3 

Sodium (Na) 77.8 

Magnesium (Mg) 4.3 

Calcium (Ca) 14.9 

Iron and alumina (Fe 2 3 , A1 2 3 ) 7.0 

Chlorine (CI) 17.5 

Sulphuric acid (S0 4 ) 27.6 

Carbonic acid (HC0 3 ) 212.7 

Silica (SiO*) 28.1 



393.2 



HARRIS AND VICINITY. 



B. B. Comer's well, Harris; bored by W. L. Morrison it 
1899; record furnished by him; depth, 780 1-2 feet. 

Record of B. B. Comer's well, Harris. 



Feet. 

Clay — 4 

Coarse sand 4 — 20 

Blue marl 20 — 120 

Shell rock 120 — 120% 

Sand 120% — 130 

Soft rock 130 — 133 

White sand with plenty of water containing 

white sediment; not good; cased off 133 — 153 

Soft shell rock and hard marly sand 153 — 220 

Blue marl 220 — 550 

Hard blue sand 550 — 600 

Marly sand and shell rock alternating; no 

more water 600 — 780 



C. H. Bishop's well, Harris; bored in September 1899, by 
W. L,. Morrison ; record furnished by him ; depth, 183 feet ; 
water rises to — 10 feet; pump put down to 120 feet; yield, 6 
gallons per minute by pump. 

Record of C. H. Bishop's well, Harris. 



Feet. 

Clay and sand — 13 

Marl 13 — 103 

Hard shell rock 103 — 105 

Marl 105 — 110 

Shell rock 110 — 112 

Water-bearing sands 112 — 115 

Shell rock and marl alternating 115 — 140 

Compact marl 140 — 183 



WATERS 01? THE CRETACEOUS. 243 

The analysis by Mr. Hodges shows this water to have the 
following- composition : 

Analysis of water from G. H. Bishop's well, Harris. 



Parts per million. 

Potassium (K) 3.8 

Sodium (Na) 85.3 

Magnesium (Mgj 5.1 

Calcium (Ca) 9.3 

Iron and alumina (Fe 2 3 . Al«O s ) 5.3 

Chlorine (CI) 17.5 

Sulphuric acid (SOJ 31.6 

Carbonic acid (HCOs) 211.6 

Silica (Si0 2 ) 18.9 

38S.4 



B.- B. Comer's wells, all bored by D. A. Sylvester: No. 1. at Harris Sta- 
tion, 150 yards from depot; depth, 62 feet; casing, 3-inch, to marl; first 
water, at 55 feet, stands at 9 feet above the surface; original flow, 7 
gallons per minute at 2 feet above the surface; present flow, one-eighth 
gallon, per minute. Record: Soil, 0-16 feet; marl, 16-55 feet; sand, 55-62 
feet; thin shell rock at 52 feet. No. 2, 75 yards west of Harris Station, 
on higher ground than No. 1; bored in 1904; depth, 110 feet; casing, 3-inch 
to marl; first water at 107 feet, stood at -14 feet. Record: Soil, 0-17 feet; 
marl, 17-107 feet; sand, 107-110 feet. No. 3, 300 yards north of west of 
Harris Station; bored in 1904; depth, 108 feet; casing, 3-inch; first water, 
at 100 feet, stood at surface; second water, at 106 feet; original flow, one- 
half gallon per minute; present flow, one-sixth gallon per minute; tem- 
perature, 68°. Record: Sand, 10-17 feet; marl, 17-100 feet; sand, 100-103 
feet; rock, 103-106 feet; sand, 106-108 feet. No. 4, 1 mile south of Harris 
Station; bored in 1904; depth, 139 feet; casing, 3-inch; first water at 134 
feet; original flow, 3y 2 gallons per minute; present flow, 3 gallons per 
minute; temperature, 66°. No. 5, 4 miles southwest of Harris Station; 
bored in 1904; depth, 201 feet; casing, 3-inch; first water, at 197 feet; rose 
to 3 feet above the surface; original flow, 3 gallons per minute; present 
flow, 2V£ gallons per minute; strong of sulphur; temperature, 68°. No. 
6, 150 yards west of No. 5;. bored in 1904; depth, 184 feet; first water at 
180 feet, rose to 3 feet above the surface; original flow, 2 1-2 gallons per 
minute; present flow, \ x / 2 gallons per minute; thin shell rock at 90 and 
135 feet; strong of sulphur; temperature, 6iy 2 °. No. 7, 5 miles southwest 
of Harris Station; bored in 1904; casing, 3-inch; first water at 164 feet; 
rose to 3 feet above the surface; flow, 6 gallons per minute. No. 8, 3 
miles southeast of Harris Station; bored in 1904; depth, 218 feet; first 
water at 208 feet; second water, at 215 feet, stood at -9y 2 feet. Record: 
Sand and clay, 0-37 feet; marl with much sand, 37-42 feet; hard rock, 42-43 
feet; marl with sand, 43-215 feet; so much sand mixed with tne marl that 
the well had to be cased to the bottom. No. 9, 4 miles west of north 
of Cowikee; bored in 1902; depth, 105 feet; first water at 158 feet; second 
water, at 160 feet; rose to 2 feet above the surface; original flow, 2 gal- 
lons per minute; present flow, iy 2 gallons per minute; temperature, 69°. 
No. 10, three-fourths mile northeast of No. 9; bored in 1904; depth, 19S 
feet (?); record unreliable. No. 11, one-half mile west of No. 9; bored in 
1902; depth, 330 feet; first water, at 326 feet; stands at -22 feet; tastes of 



244 details: coastal plain division. 

alum. No. 12, one-half mile northwest of No. 11; bored in 1902; depth, 
370 feet; first water at 355 feet; second water, at 363 feet, stands at -26 
feet. No. 13, 1 mile west of No. 9; bored in 1S04; depth, 170 feet; first 
water, at 164 feet, rose to 4 feet above the surface; original flow, 3% gal- 
lons per minute; present flow, 3 gallons per minute; tempera tur, .67°. 
No. 1-i, on Cody place, 300 yards east of No. 10; bored in 1904; depth, 171 
feet; record same as No. 10. No. 15, 2% miles northeast of Cowikee; bored 
in 1902; depth, 270 feet; first water, at 166 feet; flow, 2 gallons per minute; 
temperature, 69°. No. 16, 4 miles east of Cowikee; bored in 1902; 3 wells 
here on Richardson place; same record as No. 15; flow, 4 gallons per 
minute; temperature, 69°. No. 17, located 7 miles north of east of Cowi- 
kee; fcored in 1S02; depth, 280 feet; first water, at 274 feet; stood at -19 
feet. 
Well at Spring Hill, Cowikee; depth, 600 feet; water stands at -18 feet. 



City well, bored by Y. T. Radford in 1903; depth, 560 feet; cased to bot- 
tom, 4-inch, 6-inch, 8-inch, and 12-inch; first water, at 520 feet; stood at 
-252 feet. Record: Clay, 0-50 feet; sand. 50-80 feet; yellow clay, 80-120 feet; 
quicksand 120-220 feet; rock and marl, 220-520 feet; sand and water, 520-560 
feet. 

The character of the water from this well is shown by the analysis 
below, made by Mr. Hodges: 

Analysis of water from city well, Clayton. 



Parts per million. 

Potassium (K) 4.6 

Sodium (Na) 69.4 

Magnesium (Mg) 2.9 

Calcium (Ca) 19.5 

Iron and alumina (Fe 2 3 , A1 2 3 ) 6.5 

Chlorine (CI) 21.2 

Sulphuric acid (SO. t ) 25.7 

Carbonic acid (HCO s ) 195.5 

Silica (Si0 2 ) 26.8 

372.1 



waters of the tertiary 245 

Waters of the Tertiary. 
general statement. 

As has been stated, (p. no), the number of artesian wells in 
the Tertiary area is as yet comparatively small, and the data 
are not at hand for defining the artesian horizons with the 
precision that is possible in the case of some parts of the Cre- 
taceous. A general account of the character and succession 
of the Tertiary strata has been presented in Chapter I (pp. 
4-25). To this account is here added a more extended consid- 
eration of these beds in their relations to underground waters, 
especially artesian. 

The Clayton limestone, at the base of the Tertiary, seems 
nowhere to be of importance as an artesian horizon, but in the 
eastern counties its occurrence is of such magnitude as to give 
rise to underground, cavern-conducted streams and their at- 
tendant "big springs." 

The great body of Sucarnochee clays, next above the Clay- 
ten, is also wholly unsuited to the absorption and storage of 
the rainfall. They underlie, in Alabama and Mississippi, the 
"Flatwods," or "Post Oaks," in which the soils are generally 
tough and intractable, badly drained, and thus difficult of cul- 
tivation. All this region is deficient in good water, and very 
much of it is waste land. 

Between these Flatwoods clays and the base of the Clai- 
borne, is a great thickness — 750 feet or more — of sands and 
clays and sandy clays, interspersed with beds of lignite and 
deposits of marine shells. These constitute the Chickasaw 
(Wilcox) division of the Tertiary, or Lignitic, as it was for- 
merly called, throughout which the conditions are more or less 
favorable to artesian systems; for, while most of the strata 
are sandy, yet interspersed throughout their entire thickness 
are beds of clay and of indurated calcareous sands, so disposed 
as to confine the waters which may have permeated and filled 
the more sandy strata. Bored wells at the proper altitudes 
throughout this whole territory should, therefore, yield water 
from depths varying locally. 



246 details: coastal plain division. 

It has been found by experience that in the Chickasaw or 
Lignitic division the Nanafalia sands, together with the adja- 
cent parts of the Naheola below and the Tuscahoma above, 
form a good artesian reservoir.* At the top of this' division 
the Woods Bluff and Hatchetigbee sandy clays with indurated 
layers constitute another artesian horizon, which is drawn upon 
by a number of wells. 

The Claiborne formation, with its three members, Gosport, 
Lisbon and Buhrstone, aggregating, 400 to 450 feet in thick- 
ness, consists' of sands, interstratified in the lower (Buhrstone) 
member with beds of clay, often indurated into rock, and in the 
upper member with indurated ledges of calcareous sands. The 
whole formation is therefore well adapted, both in materials 
and structure, to serve as an artesian water horizon. Many 
wells in Georgia and Mississippi and a few in Alabama de- 
rive their waters from this reservoir. 

The St. Stephens limestone, being calcareous throughout, 
would on general principles be regarded as unfavorable for ar- 
tesian waters; but the limestone varies widely in character, 
from an open, porous rock to a very compact limestone capable 
of taking a fine polish ; and experience has' shown that it fur- 
nishes the water supply of a number of artesian wells. 

The marine Tertiary beds of Miocene and later age do not 
appear at the surface to any great extent anywhere in Ala- 
bama, being covered by the Grand Gulf and Lafayette beds ; 
but the wells in Mobile and Baldwin counties have amply dem- 
onstrated the fact that they are fine water reservoirs, though 
the water is often impregnated with salt. 

Throughout the entire region underlain by the above-men- 
tioned strata the prevalence of sands in the residual soils, as 
well as in the later Lafayette ?nd Grand Gulf, which cover so 
much of the territory, has generally insured an abundance of 
good water, breaking out along hillsides as springs or within 
easy reach in shallow wells, and thus the necessity has not been 
felt for seeking water by artesian borings. 

This review of the Tertiary formations in Alabama leads 
to the conclusion that artesian water should be obtained from 
almost anv horizon above the Sucarnochee clavs. It will be 



*In the map of the Artesian Systems (Plate XIII), the water 
horizon designated as Nanafalia, is meant to include also adjacent 
parts of the Naheola and Tuscahoma. 



GEOLOGICAL SURVEY OF ALABAMA. UNDERGROUND WATER RESOURCES, PLATE XVII. 



>' 




A. Blue Pond— Near Dixie, Covington County. 




Pavilion of Sulphur Well, Near Jackson, Clarke County. 



WATERS OF THE TERTIARY 217 

seen further that there is in the Tertiary terranes no area in 
which the water conditions are dominated by a limestone of 
great thickness, like the Selma chalk of the Cretaceous. As a 
consequence there is no belt across the State within the limits 
of the Tertiary that can be compared with the chalk area in 
regard to the number of artesian wells and the conditions 
which make them almost a necessity. The nearest approach 
thereto is in the Flatwoods, or Post Oaks, underlain by the 
Sucarnochee clays ; and here the parallel extends mainly to the 
dearth of shallow waters in both sections. In the one case the 
strata are limestones of various kinds ; in the other they are 
clays ; in both the shallow waters are in excess in the winttr 
months and almost entirely absent during the dry seas'on ; in 
both water for domestic use is stored in cisterns excavated in 
the country rock, limestone or clay. 

The fact that the limestone soils of the Cretaceous are 
among the most productive in the State, has been the cause of 
the early settling of the Cretaceous region and the earlv re- 
course to artesian borings to supply human needs. In the 
Flatwoods, on the other hand, the native fertility of the soil 
las not been so immediately apparent, for the country is 
lacliy drained and difficult of cultivation and hence not much 
rproved; but the farmers are beginning to apprceiat : the 
Potential value of these lands, and deep borings are being made 
in mcreasing numbers to supply the greaie? 1 - deficiency of the 
region-good water. 

The typical Flatwods in Alabama are in Sumter and Ma- 
rengo counties, the underlying black clays becoming gradually 
more calcareous toward the east, so that across Alabama River 
in Wilcox Count}-, the tough, intractable Flatwoods clays are 
replaced by highly calcareous clays which weather into fine. 
black prairie soils. The water-bearing strata for artesian 
wells of moderate depth in the Flatwoods, as well as in the 
Wilcox County prairie lands, are the Ripley beds, which on 
the outcrop are hardly more than loose sands, the lime having 
been leached out of them; below water level, however, the\ 
may be compact calcareous sandstones, comparatively imper- 
meable. 

In several counties in northeastern Mississippi, where the 
same conditions prevail, wells bored in the Flatwoods reach 
water at reasonable depths, the water rising not to the surface, 



248 details: coastal plain division. 

but within pumping- distance. In Sumter County, Ala., also, 
there are several old wells in the Flatwoods with the water 
standing within 100 feet of the surface; in Marengo County 
several wells 350 to 800 feet deep have been put down in the 
Flatwods region and the water stands in them within 40 to 60 
feet of the surface. During the past twelve months deep wells 
in the Flatwods have been sunk through the Selma chalk and 
obtained water from the underlying Eutaw sands. In one in- 
stance, viz., at Gates in Marengo county, overflowing water, 
25 gallons per minute, was reached at 1120 feet depth. It 
seems therefore in the highest degree probable that artesian 
water may be obtained in almost any part of the Flatwoods, 
at depths varying from 300 to 1100 or 1200 feet. The shal- 
lower wells have not as yet yielded overflowing water, but 
those which penetrate into the Eutaw sands' are likely to get it. 

With an abundance of good water for domestic purposes, 
the Flatwoods, heretofore allowed to lie uncultivated, would 
become desirable farming lands in places where proper drain- 
age is practicable. 

In the area underlain by the St. Stephens limestone there 
is, as a rule, no actual need of artesian borings for a water 
supply. In Washington, Choctaw, and Clarke counties, how- 
ever, by reason of the Hatchetigbee anticlinal uplift, this for- 
mation lies at the surface through a belt of considerable width. 
In this belt the presence of black limy soils and the 'dearth oi' 
surface waters present similar conditions to those in the ter- 
ritory of the Selma chalk, and here also artesian wells are nu- 
merous. This is especially the case in Clarke and Wayne coun- 
ties, Mississippi, at the west end of this anticline, where it is 
crossed by the Mobile and Ohio Railroad, the towns of Shu- 
buta, Waynesboro, and Winchester being supplied by arte- 
sian wells going clown into the underlying Claiborne beds. 
In Alabama there are few artesian wells in this belt, partly at 
least for the reason that it is not crossed by a railroad line 
and has few towns of considerable size. 

South of the outcrop of the St. Stephens limestone, except in 
a few places, the only formations appearing at the surface are 
the Grand Gulf, the Lafayette, and the later sands of the bot- 
tom lands and parts of the coast, the shallow waters being found 
almost exclusively in the two first named. The Lafayette will 
be referred to 1 in connection with shallow waters in almost 



WATERS OF Tun ti;rti.\rv 2-1 W 

every county in the Tertiary division of the Coastal Plain, and 
further description of it here is unnecessary ; but because of 
the preponderating' influence of the Grand Gulf in some of the 
lower counties — Washington, Mobile, Baldwin, Escambia, and 
Covington — a fuller account oi it and of the late Tertiary for- 
mations hidden underneath it will be presented at this point. 
This account will be made clearer by Plates XVI to XXII 
referred to below, which show the variations in the formation 
due to geographic distribution. Plate XVI, B, illustrates the 
relations of the strata north of Alabama River at Gainestown, 
Clarke County. Here the Grand Gulf overlies the St. Steph- 
ens limestone, which may be seen in all the low bluffs a short 
distance back from the river bottom. The Grand Gulf, which 
consists of sands with intercalated beds of clay, is in its turn 
overlain by a capping of Lafayette red loam and pebbles'. None 
of the St. Stephens is shown in the view r , but it outcrops a 
few hundred yards distant from this locality. In those parts 
of the Grand Gulf terrane, where the limestone is near the sur- 
face, lime-sinks and consequent deep ponds are common and 
characteristic. The view T of Blue Pond, in Covington count)", 
near Dixie P. O. Plate XVII, A, shows a rather exceptional 
type of these limesink ponds, in that its formation has been of 
such recent date that the banks are not yet rounded up by 
weathering but remain nearly vertical. It gives, however, the 
plainest evidence of its origin. Usually the sinks are not so 
sharply defined because of the wearing down and filling in 
around the edges, and the lakes or ponds take on the character- 
istics of the lakes so numerous in Florida. These occur where 
the limestone is not very deep below the surface and is covered 
by the Grand Gulf and Lafayette materials. Only one of this 
class' of pond is known in Alabama and that is McDacle's 
Pond near Florala, close to the Florida-Alabama line in Cov- 
ington county, and shown in Plate XXIII. 

To the south the St. Stephens limestone sinks deeper and 
deeper below the surface and its influence on the topography 
gradually dies out. Other later Teftiarv (Miocene) marine 
beds, many feet in thickness, come in above the limestone as 
it sinks. These later beds are exposed at comparatively few' 
places, but their presence is amply demonstrated by all the deep 
borings' in Mobile, Baldwin, and Escambia counties, at Oak 
Grove, Fla., and along Chattahoochee River. 



250 details: coastal plain division. 

Above these marine beds, apparently with nearly if not quite 
horizontal stratification, lie the two great surface formations of 
the Coastal Plain— the Grand Gulf and the Lafayette — practi- 
cally unchanged in materials and stratification down to the ' 
very borders of the bays' on the Gulf of Mexico. High bluffs 
of Grand Gulf material capped with the Lafayette, overlook 
these bays at many points where deep borings reveal the pres- 
ence of Miocene shell beds 700 to 1500 feet or more below. At 
Montrose, on Mobile Bay, between Daphne and Point Clear, 
there is a fine exposure of the two formations, as shown in 
Plate XVIII. The capping of Lafayette red loam and pebbles 
is clearly distinguishable from the main mass of the bluff, 
which is made by the sands' and laminated clays of the Grand 
Gulf. The unconformity between the two formations is also 
very clearly shown in this view where the indurated layer in 
the Grand Gulf, many feet below the Lafayette at the left of 
the view, is in contact with it at the extreme right, the Lafayette 
following the contour of the surface while the Grand Gulf is 
nearly horizontal in stratification. So far as can be seen the 
materials' here are similar to those at Gainestown Ferry. 

Similar unconformities may be seen at many points in Alaba- 
ma and Mississippi, for the Lafayette seems to have been spread 
over the surface of the country after it had attained approxi- 
mately its present relief. On Perdido Bay, from Lillian to Sol- 
dier Creek Post office, and probably at many other points not 
visited by the writer, these same formations make high bluffs 
coming down to the water's edge. (Plates XIX and XX). 
The character and arrangement of the materials of the two 
formations along Perdido Bay are not essentially different from 
what may be seen at Montrose. , 

A few words may be said in regard to the surface features 
of these highlands, which, as is' shown in the views just referred 
to, extend clown to salt water. South of the belt in which the 
underlying St. Stephens causes the lime-sinks and ponds, the 
general surface down to the Gulf is that of a plateau, the high, 
flat lands being well adapted for farming and grazing, but now 
devoted practically to two industries — timber and turpentine. 
The monotony of these high, flat lands is, however, everywhere 
interrupted by shallow depressions or sinks, few of them ex- 
ceeding 4 or 5 feet in depth. Water may collect in these de- 
pressions, forming ponds a few yards to 40 or 50 yards in di- 



WATERS OF THE TERTIARY 25] 

ameter, around which a shrubby growth of gums may spring 
up (PL XXI.) Other depressions, in many cases larger than 
the ponds, may be void of shrubby undergrowth or of stand- 
ing water, and thus give rise to savannahs or pine meadows, as 
shown in Plate XXII. The latter term is often applied to 
lower lying lands timbered with longleaf and Cuban pine. The 
savannahs grade into more undulating lands which with their 
growth of high grass and bright flowers and absence of dis- 
figuring undergrowth give the impression of being well kept 
parks. Through these parks one may drive for miles in al- 
most any direction without need of road or path. In the sa- 
vannahs the growth of pine is stunted ; in the park lands' it is 
better, but not of the best. 

There is some doubt as to the cause of these depressions, 
which are characteristic in Florida, Georgia, Alabama, Miss- 
issippi, and presumably in the other Gulf States. They seem, 
however, to be due to inequalities in the surface of the under- 
lying Grand Gulf clays, since there are generally no underlying 
limestones or other soluble materials near enough to the surface 
to cause the formation of so many small depressions of limited 
extent within, say. an acre of territory. 

The above account will, it is thought, better than any other 
description, show the absolute dependence of the shallow-water 
conditions in the lower counties on the two late formations 
which have so much in common, both being spread, with no ap- 
preciable prevailing dip, over the beveled edges of the south- 
ward-dipping St. Stephens and later Tertiary formations. 

The artesian conditions' in this territory are fixed by the un- 
derlying Tertiary formations above mentioned. That they are 
generally favorable is demonstrated by the success of borings 
in Escambia and Mobile counties, very few having been made 
in the other counties where similar conditions prevail. 



252 details: coastal plain division, 

discussion by counties. 
henry county. 

Surface Features. 

The older Tertiary formations which underlie the territory 
of Henry County include the Nanafalia sands and the Hatche- 
tigbee and Claiborne, all of which in other places are good arte- 
sian reservoirs. Over the greater part of the county there are, 
in addition to the above, two more recent formations, the Grand 
Gulf and the Lafayette, in the materials of which is stored a 
generous supply of surface water to be drawn on by springs and 
shallow weils'. There is no lack, therefore, of good freestone 
waters in most parts of the county. With proper selection of 
altitude, there should be no trouble in getting artesian water 
from the deeper beds. 

Artesian Record. 

The record of only one deep well in Henry County has been 
obtained — the town well at Abbeville ; bored by Van Vleet in 
1904; depth, 401 feet; water stands at — 172 feet; pump yields 
60 gallons per minute for seven hours. The formation at the 
surface is the Buhrstone and the boring penetrates probably 
into Tuscahoma or Nanafalia sands. 

HOUSTON COUNTY. 
Surface Features. 

The surface of new county of Houston is covered in many 
parts by the red sandy loams and pebble beds of the Lafayette. 
Below these are the sands and stratified clays of the Grand 
Gulf, and under them the white St. Stephens' limestone. The 
last-named formation underlies the entire area of the county 
except some small tracts in the extreme northern part and 
along Chattahoochee River about Columbia. 

Owing to the character of the two surface formations the 
water supply from wells and springs is in geneial good in 
quality and adequate in quantity. 



waters m' the; tertiary 253 

Artesian Records. 

Deep wells are recorded from two points only — Columbia 
and Dothan. 

COLUMBIA. 

Columbia is' situated on the terrace of Chattahoochee River 
in the Claiborne formation. 

Well bored by Harrington about 1890 or 1891; depth. 485 feet; casing. 
8-inch and 6-inch, to bottom; water rose to -8 feet, and an excavation 
of 11 feet was made around the well to obtain a flow; yield, 50 gallons 
per minute; considered very fine water; analysis shows magnesia. Rec- 
ord: Marl near the top about 150 feet thick; hard shell rock at frequent 
intervals below to the bottom; probably in Nanafalia sands. 



City Wa,ter Company's wells: No. 1, bcred by C. A. Ray, of Providence. 
R. I., in 1S96; depth, 625 feet; water stands at -150 feet; yield with air 
life, 2C0 gallons per minute; water excellent; casing, 8-inch to about 300 
feet; remainder 6-inch; flow has increased; present yield, 250 gallons per 
minute; temperature, 72°. No. 2, bored 5 feet from No. 1; depth unknown; 
no water obtained. 

Town well, in Section 24, Township 3, Range 26; bored by S. S. Chandler 
in 1903; depth, 645 feet; casing, 425 feet 8-inch; 210 feet 6-inch; first water 
at 360 feet, stood at -75 feet; second water, at 600 feet, stands at -130 feet; 
air-life gives 250 gallons per minute; level lowered to -150 feet. 

Record of toivn well, Dothan. 



Feet. 

Clay — 20 

Sand 20 — 177 

Sand rock 177 — 239 

Dry sand 239 — 217 

Sand rock 247 — 267 

Dry sand 267 — 344 

Sand rock 344 — 395 

Sand 395 - 511 

Sand rock 511 — 517 

Sand and water 517 — 640 



Ice Company's well, bored by Frank Sutter in 1904; depth, 622 feet; 
casing. 0-200 feet, 8-inch; 200-495 feet 6-inch; first water, at 400 (?) feet, 
stood at -60 feet, small supply; second water, at 622 feet, stands at -70 
feet;pumping level, -150 feet; yield, 50 gallons per minute. Record: 
Clay, 0-100 feet; coarse gravel, 100-102 feet; sand, 102-210 feet; sand with 
layers of soft rock from 1 inch to 6 feet in thickness, 210-575 feet; dry 
sand. 575-6C0 feet; clay. 600-622 feet; sand at 622 feet. 

Dothan is on the St. Stephens formation and these borings probably go 
down into the Nanafalia sands. 



•254 DETAILS : COASTAL PLAIN DIVISION. 

GENEVA COUNTY. 
Surface Features. 

Geneva County lies practically wholly within the territory 
of the St. Stephens limestone, but the Tertiary rocks, instead 
of dipping uniformly southward, lie in undulations which bring- 
the strata of the Claiborne to the surface along the banks of 
Pea River, even as far as the town of Geneva, near the southern 
border of the county. For this reason it is not easy to deter- 
mine the horizon to which the bored wells penetrate. 

Over the older Tertiary rocks lie, as usual in this part of the 
State, the Grand Gulf sands and stratified clays in variable 
thickness, and upon these, where not removed by erosion, the 
Lafayette red s'andy loams and pebble beds. These two later 
formations afford favorable conditions for abundant supplies 
of good surface water from wells and springs. At Coffee 
Springs there are several magnificent springs boiling up 
through the sands and running off in a brook of good size. 

Artesian Records. 

The artesian wells of Geneva County do not flow, probably 
because of the lack of head due to the irregularities in the dip 
of the Tertiary strata. The supply, however, seems to be am- 
ple, the water in most of them being in all probability obtained 
from the strata of the Buhrstone. But few records have been 
collected since the boring of deep wells, except at the town 
of Geneva, began only on the completion of the branch of the 
Central of Georgia railway through the county a few years ago. 

The wells at Hartford and Slocomb begin in the St. Steph- 
ens' and reach the base of the Claiborne or the upper part of the 
Buhrstone. 

GENEVA. 

Public well, bored by W. L. Morrison in 1900; water, at 307 feet, rose to 
-14 feet, the supply appearing inexhaustible; but through some dissatis- 
faction the city council insisted on boring deeper, with the resul that 
the. casing was broken, the flow lost, and the well Anally abandoned. 
Record: Coarse white and yellow sand, 0-30 feet; yellow marl, 30-42 feet; 
bluish sand, 42-80 feet; buhrstone, (?) soft in middle, 80-84 feet; blue sand, 
84-94 feet; shell rock, 94-98 feet; sand and coral rock alternating, 96-338 
feet. The bottom of the boring was probably in the Buhrstone or the 
underlying Hatehetigbee. 



WATERS OK THE TERTIARY 255 

Town well, bored by S. S. Chandler in 1903; depth, 261 feet; casing, 108 
feet 10-inch, 148 feet 8-inch; first water, at 129 feet, stood at -10 feet; 
second water, at 216 feet, stood at -12 feet; air lift used; yield (estimated), 
60 gallons per minute. Record: Sand, 0-108 feet; lime rock (probably Clai- 
borne), 108-129 feet; gravel, first water. 129-133 feet; marl, 133-183 feet; lime 
rock (probably Claiborne). 183-250 feet; sand, second water, 250-261 feet. 

Besides these, several shallow artesian wells have been sunk 
in Geneva, a typical one supplying the railroad tank near the 
river. The boring goes down 8o feet below the level of the 
track, getting water from below the first rocky or limestone 
ledge, with a stand of — 12 or — 15 feet. A well several feet 
in diameter is sunk to this point and bricked up. A pump de- 
livering between 4000 and 5000 gallons per hour holds the level 
of the water at a constant point, which represents the capacity 
of the well. The water is quite pure and soft and free from 
taste of any kind. 

HARTFORD. 

Town well, bored by W. C. Van Vleet in 1904; depth, 314 feet; first water 
at 200 feet; second water, at 314 feet, stands at -18 feet; estimated yield, 
1C0 g-allons per minute for three days; pumping level, -25 feet. 

SLOCOMB. 

Morris Lumber Company's well, bored in 1901 by the mill hands; depth. 
280 feet; casing, 160 feet, 6-inch; water stands at -28 feet; pump delivers 
50 gallons per minute. 



DALE COUNTY. 
Artesian Prospects. 

Dale County shows a great range in the Tertiary formations, 
which extend from the Nanafalia to the St. Stephens limestone, 
all of them covered, in places at least, by the two later forma- 
tions' so often mentioned, the Grand Gulf and the Lafayette. 
There are correspondingly great possibilities in its water re- 
sources, both surface and artesian. As yet, however, artesian 
boring has been done only at Ozark the county seat, which is 
on the outcrop of the Woods Bluff marl. At the depth of 7 to 
feet the boring must be near the base of the Tertiary, if not in 
the underlying Ripley. 



256 DETAILS : COASTAL PLAIN DIVISION. 



Town well, altitude about 8 feet below that of the Railroad track; 
bored by W. E. Hughes, of Specialty Well Drilling- Company, Atlanta, 
Ga., in 1902; depth, 710 feet; first water at 250 v ?) feet; second water 
at 710 feet; capacity of well by air lift, 200 gallons per minute. Record: 
Red clay, 0-40 feet; marl, 40-500 feet; sand, marl and shell rock (prob- 
ably the shell bed of the Nanafalia), 500-525 feet; 525-710 feet not recorded, 
or at least the record not obtained; boring probably ends ?xi the Clay- 
ton. An analysis of the water from this well has been made by Mr. 
Hodges, as follows: 

Analysis of water from town well, Ozark. 



Parts per million. 

Potassium (K) 2.9 

Sodium (Na) 6.1 

Magnesium (Mg) 7.7 

Calcium (Ca) 47.7 

Iron and alumina (Fe 2 3 , A1 2 3 ) 1.4 

Chlorine (CI) 3.5 

Sulphuric acid (S0 4 ) 8.8 

Carbonic acid (HCO s ) 132.9 

Silica (Si0 2 ) . . . . ; 45.3 

256.3 ■ 



COFFEE COUNTY. 
Surface Featuees. 

The underlying- older Tertiary formations of Coffee County 
range from the Nanafalia member of the Lignitic in the north 
to the St. Stephens limestone in the extreme south. Over all 
these are found locally remnants of the Lafayette sands, loams, 
and pebbles. 

Artesian Prospects. 

Artesian borings have been made, so far as information has 
been obtained, only at Elba, Brockton, and Enterprise. The well 
bored in 1904 at Elba gets water in the Nanafalia sands, as 
shown by the shells' brought up with the borings. The Enter- 
prise well probably goes no deeper than the Hatchetigbee sands 
underlying the Burstone. The shallower wells at Elba, 160 
to 18.S feet deep, hardly go- deeper than. the Hatchetigbee or 
Woods Bluff horizon, or perhaps into the upper part of the 
Tuscahoma sands, the town itself being on Hatchetigbee strata. 



WATERS OF THE TERTIARY 257 

ELBA AM) VICINITY. 

The most instructive of the wells at Elba is' that at the rail- 
road depot, bored by S. S. Chandler in 1904; depth, reached 
in the latter part of July, 293 feet; diameter, 12 inches, reduced 
to 10. Record: Surface sands, 0-16 feet; marl or laminated 
grayish blue clays, 16-265 feet; water-bearing sands with shells 
of Gryphaea thirsae, 265-293 feet. These shells show that the 
horizon is the Nanafalia. 

Public well, bored at the Elba court-house in 1899 by W. L. Morrison: 
flow, 2% gallons per minute at a depth of 150 feet; water now stands 
just at the surface; temperature. 68°. Record: Yellow clay, 2 feet; coarse 
yellow sand, 16 feet; blue compact marl. 42 feet; hard lignitic material. 
40 feet; blue marl, 30 feet; sand and lignite to the bottom at 150 feet. Other 
deep wells have been sunk by the same driller in this locality. 

Well 4 miles west of Elba, on an elevation about 112 feet above the 
town; bored by W. L. Morrison in 1899; water rises to -40 feet, an un- 
limited supply being obtained by the use of pumps; tastes of alum. 
Record: Red clay, 0-8 feet; coarse yellow sand, 8-30 feet; hard blacK 
rock, 30-35 feet; coarse yellow sand, 35-70 feet; shell rock, 70-72 feet; 
marl, 72-250 feet; hard rock and sand, 250-312 feet. Water supply prob- 
ably from Nanafalia sands or lower Tuscahoma. 

Several other wells were bored in 1899 and 1900 by Morri- 
son, in and around Elba. All have about the same record ; 
some are or were flowing ; in others the water stands at the level 
of the ground, or slightly below. Every new well lessens the 
flow of the others. Among these wells are those of the county 
jail; N. W. Wright; William Rushing; John Rushing; (in this 
well a log was encountered at a depth of 40 feet) ; Judge S. M. 
Rushing (this well yields 3 gallons - per minute) ; W. M. Rush- 
ing; D. C. Collins; King & Simmons; Alien King; public 
school ; W r . B. Perdue ; Mr. Lightner ; Raynor livery stable ; 
Mrs. S. E. Beard; John Farriss ; T. J. Ham; William Ham; 
J. N. Ham ; J. T. Law ; Dr. Bradley ; Dr. Boyd ; Dr. Blue ; Mrs. 
Ada Rushing ; county poor house ; Fayette Prescott ; Aaron 
Head ; W. M. Tucker ; G. W. Gunter. 

BROCKTON. 

Well 1 mile south of Brockton, at Henderson & Boyd's saw mill; bored 
by Mr. Van Vleet.. water stands at -150 feet; supply probably from the 
Nanafalia sands. 



258 DETAILS : COASTAL PLAIN DIVISION. 



ENTERPRISE. 

Town well, bored by Frank Sutter in 1903; depth, 398 feet; casing, 6-inch; 
first water, at 132 feet, stood at -132 feet; second water, at 370 feet, stood 
at -127 feet; yield, 400 gallons per minute with air lift; level lowered 12 
feet. Record: Clay, 0-60 feet; soft lime rock, 60-68 feet; shell rock, 68-98 
feet; shell rock 98-104 feet; black mud, 104-130 feet; flint rock, 130-132 feet; 
sand, 132-140 feet; marl, 140-230 feet; mud, 230-265 feet; rock, 265-266 feet; 
marl, 266-370 feet; sand and water, 370-398 feet. The following analysis 
of the water has been made by the Southern Cotton Oil Company, Sa- 
vannah, Ga.* 

Analysis of toater from town well, Enterprise. 



Parts per million. 

Sodium (Na) 17.21 

Magnesium (Mg) .74 

Calcium . (Ca) 35.17 

Chlorine (CI) 15.02 

Sulphuric acid (S0 4 ) 40.15 

Carbonic acid (C0 3 ) 39.12 

Iron and alumina (Feo0 3 ), A1 2 3 ) 8.90 

Silica (Si0 2 ) 19.50 

Volatile matter ■ 33.87 

205.25 



COVINGTON COUNTY. 
Surface Features. 

The older Tertiary formations in Covington county range 
from the Nanafalia member of the Lignitic up to the St. Steph- 
ens limestone. Unconformably overlying the St. Stephens, 
Claiborne, and Buhrstone are the sands and stratified clays of 
the Grand Gulf, capped in turn by the red loam and pebbles 
of the Lafayette where denudation has not removed them. 
Like all the counties of this latitude, Covington is well watered, 
and artesian wells are few in number and of a recent date. 

Shallow Waters. 
r 

While the character of the shallow waters is in great measure 
determined by the loose materials of the Grand Gulf and La- 



*Expressed by analyst in grains per gallon and in hypothetical 
combinations; recomputed in ionic form and parts per million at 
U. S. Geological Survey. 



WATERS OF THE TERTIARY 259 

fayettc, yet in the lower parts of Covington and adjoining coun- 
ties, and in still greater measure in Florida, these waters' are 
modified by the underlying St. Stephens limestone, and big 
limestone springs running off in veritable creeks are not un- 
common. Akin to these are the lime sinks, ponds, and lakes of 
this section. Near the western limit of Covington County, in 
Section 6, Township 2, Range 14, is' Blue Pond, with nearly 
perpendicular sides as if it had recently fallen in. The name 
characterizes the water, which is of beautiful blue color. The 
pond is hardly more than 100 yards in diameter and the water 
is about 10 feet below the general surface of the ground. 
PI. XVII, A, shows this curious pond. At Florala in the 
lower part of the county close to the Florida line is McDade's 
pond shown in Plate XXIII. This is' also of limesink origin 
but on larger scale and of greater antiquity, and illustrates a 
type of pond or lake exceedingly characteristic of many parts 
of Florida, but, so far as known, unique in Alabama. 

Artesian Prospects. 

The deepest of the artesian wells in Covington County is that 
bored for the cotton-oil mill at Andalusia, which probably goes 
down into the Nanafalia sands or perhaps into the Naheola. 
All of the wells are located geologically on the upper Claiborne 
strata, very near the contact with the Buhrstone. They are all 
likewise on or near the lines of the Louisville and Nashville 
and Central of Georgia railroads. 

ANDALUSIA AND VICINITY. 

Town well, 40 yards from Central of Georgia Railway station, in the 
N. W. quarter, N. W. quarter, Section 20, Township 4, Range 16; bored 
by Prank Sutter in 1904; casing, 8-inch and 6-inch; well was not tested 
up to the time this record was obtained; probably reaches the Tusca- 
homa or Nanafalia sands. 



2fi0 dp;tails : coastal plain division. 

Record of town well, Andalusia. 



Feet. 

Sand and clay — 113 

Sand rock 113 — 114 

Sand 114 — 122 

Sand rock 122 — 123 

Black mud 123 — 130 

Sand rock 130 — 133 

Shale 133 — 141 

Sand rock 141 — 142 

Clay 142 — 168 

Sand (at 186 feet 3 inches of rock) 168 — 186 

Clay 186 — 190 

Sand 190 — 207 

Shalv clay and sand 207 — 273 

Rock 273 — 274 

Gritty mud 274 — 313 

Gritty mud, with frequent layers of rock 313 — 380 

Blue marl 380 — 480 



Southern Cotton Oil Company's well, Audalusia, one-fourth mile east 
of station in the N. W. quarter, N. W. quarter, Section 20, Township 4, 
Range 16; bored by Prank Sutter in 1902; depth, 1130 feet; water stands 
a. -110 feet; casing 430 feet, 4%-inch; air lift gives 45 gallons per minute, 
the following analysis is by the chemist of the Southern Cotton Oil 
Company:* 



Analysis of water from Southern Cotton Oil Company's well, 
Andalusia. 



Parts per million. 

Sodium (Na) 63.84 

Magnesium (Mg) « 1.04 

Calcium (Ca) 1.23 

Chlorine (CI) 12.00 

Sulphuric acid (S0 4 7.52 

Carbonic acid (HCO s ) 72.65 

Iron (Fe) 47 

Silica (Si0 2 ) 20.52 

179.27 



RIVER FALLS AND SANFORD. 

The three following wells probably get their water from tWr 
lower strata of the Buhrstone or from the immediately underly- 



*Expressed by analyst in grains per gallon and hypothetical com- 
binations; recomputed to ionic form and parts per million at U. S. 
Geological Survey. 



WATERS OF THE TERTIARY 2') I 

ing Hatchetigbee sands, which are frequently dark colored from 
lignitic matter. 

Horse Shoe Lumber Company's well, River Falls; bored by W. M. Mor- 
rison in 1901; depth. 230 feet; yield, 3 1-4 gallons per minute. Record: 
Clay, 8 feet; coarse sand. 12 feet; yellow marl. 30 feet; alternating blue 
marl and thin layers of rock to 200 feet; buhrstone, 8 inches; water- 
bearing sands and lignite. 30 feet. 

Henderson Lumber Company's well, Sanford; bored by W. M. Morri- 
son in 1901; depth, 380 feet; casing, 3-inch; water stands at -70 feet. Rec- 
ord: Clay. 0-12 feet; white sand, 12-30 feet; hard red and yellow clay, 
30-SO feet; alternating layers of sand, blue marl and rock. 80-175 feet; 
blue marl, 175-275 feet; water-bearing sand and lignite. 275-295 feet; porous 
limestone, 2S5-350 feet; water bearing sand and rock, 350-386 feet. 

\Y. W. Vorn's well, Sanford; bored by W. lvi. Morrison in 1901; casing 
4V 2 inch; water stands at -70 feet. Record: Hard red and yellow clay, 
0-75 feet; yellow sand and soft rock, 75-90 feet; blue marl, 90-200 feet; shell 
rock, 200-202 feet; water-bearing sand, 202-235 feet. 



CRENSHAW COUNTY. 
Surface Features. 

The two northernmost townships in Crenshaw County are 
underlain by the Cretaceous formations, the rest of it by the 
Tertiary formations up to the top of the Lignitic. In the north- 
ern part of township 10, adjoining Montgomery County, the 
Selma chalk is' the surface formation, and in this vicinity wells 
would have to go through the whole thickness of the chalk to 
reach the Eutaw sands. A prominent ridge, the entension of 
the Chunnennugga Ridge of Bullock County (see p. 226), 
marks the line between the chalk and the Ripley in the lower 
part of township 10. 

Artesian Prospects. 

In the area underlain by the Ripley, embracing most of town- 
ship 9, artesian prospects are favorable, but no records of wells 
have been obtained. In the adjoining county, Pike, in the same 
formation are several wells about Orion. In the Clayton beds, 
which form the base of the Tertiary, wells usually have to go 
very deep and are frequently unsuccessful. The only records 
obtained are from townships 6 and 7, in the lower part of the 
county. It is probable that the wells about Brantley and Theba 



262 DETAILS : COASTAL PLAIN DIVISION. 

get water from the Nanafalia sands and that at Searight, from 
a higher horizon, possibly the Tuscahoma. Flowing wells are 
rare among those as yet bored. 

THEBA. 

Bently Lumbers Company's wells: No. 1, in the S. B. quarter Section 
25, Township 7, Range 17; bored by mill hands in 1904; depth, 225 feet; 
casing, 20 feet, 6-inch; first water at 177 feet; second water, at 225 feet, 
rose to 14 feet above the surface; presnt flow, 17 gallons pr minute; tem- 
perature, 68°, Record: Sand and clay, 0-18 feet; blue marl, 18-80 feet; 
sand rock, 80-81 feet; black marl, 81-90 feet; alternating layers of sand 
and rock, 6 inches thick, 90-200 feet; clay, 200-203 feet; rock, 203-204 feet; 
sand and water, 204-225 feet. No. 2, 75 yards from No. 1; bored by mill 
hands in 1903; depth, 177 feet; casing, 20 feet, 4-inch; flow, 1 gallon per 
minute; temperature, 68°. Record same as No. 1. 

BRANTLEY AND VICINITY. 

Town well, Brantley, in the N. W. quarter Section 16, Township 7, 
Range 18; bored by C. C. Brinson in 1899; depth, 366 feet; casing, 20 
feet, 4-inch; water stands at -22 feet; pump gives 20 gallons per minute 
for four hours. The character of the water from this well is shown 
by the following analysis by Mr. Hodges: 

Analysis of water from town well, Brantley. 



Parts per million. 

Potassium (K) 1.3 

Sodium (Na) 4.1 

Magnesium (Mg) 5.6 

Calcium (Ca) 45.6 

Iron and alumina (Pe 2 3 , Al 2 O s ) 9.9 

Chlorine (CD ..... 1.7 

Sulnhuric acid (SO..) 10.1 

Carbonic acid (HCO a ) < 157.5 

Silica (SiO-t 35.5 

271.3 



L. C. Cooper's well, Brantley, in the N. W. quarter Section 16, Town- 
ship 7, Range 18; bored by George Thompson in 1899; depth, 170 feet; water 
stands at -25 feet. 

Southern Cotton Oil Company's well, Brantley, in the i*. W. quarter 
Section 16, Township 7, Range 18; bored by S. W. Ingram, in 19o2; depth. 
155 feet; water stands at -18 feet. 

J. T. Cooper's well, at mill one-fourth mile east of Brantley, in the 
N. E. quarter Section 16, Township 7, Range 18; bored by George Thomp- 
son in 1899; depth, 260 feet; casing, 20 feet,, 4-inch; water stands at -22 
feet; pump gives 50 gallons per minute. 



WATERS ()!• THE TERTIARY 2Q[ 



SKAWH1GII 1'. 

Southern Cotton Oil Company's well, in the N. E. quarter Section 19, 
Township 6, Range*17; bored by S. W. Ingram; depth, 276 feet; casing, 
20 feet. 4-inch; first water small stream; second water, at 276 feet, stands 
at -12 leet; force pump gives 27 gallons per minute. 



BUTLER COUNTY. 
Surface Features. 

With the exception of a small area in the northeast corner, 
Butler County is underlain by Tertiary strata, embracing all 
the lower divisions up to the Buhrstone. In the territory of 
the Ripley and Clayton calcareous beds are prevalent and the 
topography in general is much broken because of the numerous 
indurated ledges of calcareous material among the sandier beds. 
To the south about Greenville and for several miles on either 
side, is a .great extent of red sands' or loams, which resemble 
those of the Lafayette but probably consist of residual matter 
from the Tertiary beds. 

These Tertiary formations range from the Midway up to the 
Claiborne, and in their outcrops present the usual monotonous 
character. Overlying all, where not removed by denudation, 
are the red loam and pebble beds of the Lafayette. In many 
localities these surface beds are extremely sandy, especially on 
the watersheds. An example of this condition may be noted 
along the Montgomery road between Greenville and Sandy 
Ridge. 

Mineral Waters, 
roper's well. 

One of the most widely known mineral waters of Alabama, 
sold under the name of "Wilkinson's Matchless Mineral Wa- 
ter," is obtained from Roper's well, 3 miles east of Greenville, 
and a well subsequently sunk near it. The latter well is about 
40 feet deep and 15 feet in diameter. The section shown in 
the sides of the well consists of 9 1-2 feet of sandy clay, 
6 3-4 feet of sand and mottled clay, and below this the "black 
earth," which continues to the bottom of the well. This black 



264 DETAILS : COASTAL PLAIN DIVISION. 

earth is the source of the "mineral.'' It is a dark colored sandv 
clay containing organic matter and iron pyrites, with considera- 
ble greens'and in small grains irregularly disseminated through 
it. The reaction of the oxidation products of the pyrites on the 
clay and its contained vegetable matter yields the sulphuric 
acid, the alum, and the other sulphates which characterize the 
water, as shown by the analysis. 

The water fresh from the well is colorless, the iron being 
in the ferrous condition, but on standing it gradually 
becomes yellowish red from further oxidation of the iron. 

As' the source of the mineral matter is superficial and local, 
the strength of the w r ater varies with the rainfall, being much 
less during the rainy season. Analyses may therefore differ 
very widely in regard to the amount of mineral matter to the 
gallon. An analysis made by Dr. Metz, of New Orleans, shows 
1244.45 grains; a sample of the bottled water furnished, by the 
proprietor of the well, and said to have been collected six 
years ago, contains 1333.8 grains; the water in a 16-quart bot- 
tle on sale June 1, 1905, contains 458.45 grains; while the sam- 
ple direct from the well collected by Mr. Hodges for analysis 
after several months of rainy weather, contains 213.9 grains. 
In putting up the water for the market it is the endeavor of 
the proprietor to make it as nearly as possible of uniform 
strength. When too concentrated it is diluted with fresh water : 
when too- dilute leachings from hoppers of the pyritous earth 
are added. 

Mr. Hodges' s analysis is given below ; also, for the sake of 
comparison, an analysis made by J. B. Little and the writer 
about twenty years ago, from a sample collected by Mr. Little, 
and one made by Dr. Metz, of New Orleans. These analyses 
sufficiently illustrate the variations in the concentration, as 
well as in the relative proportions of the different ingredients, 
which takes place in the course of time and by reason of sea- 
sonal changes. 



WATERS OV TI1IC Tl'UTlARY 



265 



Analyses of "Matchless Mineral Water" from Roper's well, near 

Greenville. 



n 



in 



(Parts per million.) 

I 

Potassium (K) 7.G 

Sodium (Na) 57.(5 

Magnesium (Mg) 78.0 

Calcium (Ca) 322.4 

Iron (Fe, ferrous) 90.5 

Iron (Fe, ferric) 204.1 

Aluminum (Al) 132.8 

Chlorine (CI) 78.3 

Sulphuric acid (SO,) 2493.3 

Sulphuric acid (H0SO4). free) 19.9 

Silica (SiO a ) 131.2 

3615.7 



15.8 


33.0 


51.9 


76.9 


235.1 


278.0 


300.8 


373.4 


10S5.0 


1358.8 


1038.4 


4013.7 


33.2 


69.8 


42.3 


53.2 


6434.8 15130.3 


30.7 




86.4 


103.7 


9354.4 21490.8 



I Analysis by Robert S. Hodges, 1905. 

II Analysis by J. B. Little and Dr. E. A. Smith, about 1885. 

III Analysis by Dr. Metz, of New Orleans, 1893.* 



*Originally expressed by analysts in grains per gallon and in form 
of radicals; recomputed in ionic form and parts per million by R. 
S. Hodges. 

BUTLER SPRINGS. 

Near the western border of the county, just south of Redicks 
Creek are the Butler Springs', formerly much visited, but now 
nearly abandoned, though a few families come every year with 
camping outfits and drink the water. Its character is shown 
by the following analysis by Mr. Hodges : 

Analysis of ivater from Butler Springs. 



Parts per million. 

Potassium (K) 1.8 

Sodium (Na) 9.3 

Magnesium (Mg) 1.0 

Calcium (Ca) 5.3 

Iron and alumina (Fe 2 3 . A1 2 3 ) 2.9 

Chlorine (CI) 7.0 

Sulphuric acid (S0 4 ) 13.1 

Carbonic acid (HCO a ) 16.5 

Silica (SiO») 19.6 



76.5 



266 DETAILS : COASTAL PLAIN DIVISION. 

Artesian Prospects. 

All the artesian wells in Butler are to be found along the 
line of the Louisville and Nashville railroad, and most of them 
have been bored to supply the needs of saw mills. In some 
cases' where the timber supply has been exhausted the mills 
have been moved and the wells have fallen into* decay. 

GREENVILLE. 

City waterworks wells at the foot of the hid east of town, 60 feet or 
more below the level of the railroad track, which is 444 feet; bored in 
1892 by the American Pipe Manufacturing Company; depth, 400 feet; 
water supply obtained between 186 and 217 feet; below 217 feet the strata 
were blue to black clays, alternating' with harder strata, probably of 
the Ripley formation; mouth of the well is on the Naheola sands; water 
stands at -50 feet; pump delivering 90 gallons per minute does not lower 
the stand more than one foot. According to the analysis of Mr. Barnura, 
chemist to the company, the solid matter in solution in this water, con- 
sist in the main of the carbonate and sulphate of magnesium and chlo- 
ride of sodium. » 

Ice-factory well, in the N. E. quarter N. E. quarter Section 24, Town- 
ship 10, Range 14; depth, 107 feet; casing, 84 feet; 8-inch; water stands at 
-13 feet; force pump gives 75 gallons per minute; boring probably does not 
go through the Naheola. 

Southern Cotton Oil Company's well, in the S E. quarter S. "W. quar- 
ter Section 14, Township 10, Range 14; bored by Morgan, of Birmingham, 
in 1902; depth, 105 feet; casing, 8-inch to bottom; water stands at -53 feet; 
estimated yield with steam pump, 150 gallons per minute; ends prob- 
ably in the Naheola. 

FOREST. 

W. M. Plowers's wells: No. 1. at saw mill, in the S. E. quarter Section 
8, Township 9, Range 14; bored by M. S. Gilmer, in 1892; depth, 195 feet; 
casing, 5-inch; water stands at -20 feet; first water at 195 feet; pump yields 
50 gallons per minute. No. 2, 350 yards south of No. 1; bored by M. S. 
Gilmer in 1895; depth, 390 feet; water stands at -20 feet; estimated yield 
with pump-, 50 gallons per minute. These wells are located on the Nana- 
falia outcrop and get water probably from the Naheola sands. 

BOLLING. 

W. J. Flowers Lumber Company's wells; bored fifteen years ago and 
in use about ten years; now abandoned on account of removal of the 
mill; altitude, 308 feet; depth of No 1, 1010 feet; of No. 2, 230 feet; water 
stands at -10 feet; yield, about 75 gallons per minute each, to pump. The 
water was used for steam and domestic purposes, but was not well 
adapted to the former, as it produced a scale in the boilers. As no in- 
crease in the volume of water was noticed below the depth of 230 feet, 
the second well stopped there, going down probably into the Naheola 
sands, while the deeper well may have gone to the base of the Tertiary 
or into the Ripley. 



WATERS OF THE TERTIARY 267 

CHAPMAN. 

The following wells are located near the contact of the Tus- 
cahoma and Nanafalia, and obtain water in all probability 
from the sands of the latter. ■ 

W. T. Smith Lumber Company's well, bored in 1904 by M. Canfleld; 
depth. ISO feet; flow. 150 gallons per minute. 

Louisville and Nashville Railroad well, bored in 1904 by M. Canfield; 
depth, 175 feet; flow, 150 gallons per minute. 

DUNHAM. 

Dunham Lumber Company's well, depth, 382 feet; probably obtaining 
water in th,e Nanafalia sands or the immediately underlying Naheola; 
elevation, 221 feet; water rises to 3 feet above the surface; original flow, 
18 gallons per minute; flow in 1904. about 5 gallons per minute; temper- 
ture, 73°. The record given by Mr. B. B. McKenzie is as follows: Sand 
and clay. 13 feet; marl, 160 feet; rock, 2 feet, below which a weak stream 
was struck, rising above the mouth of the well, but as the quantity 
was insufficient the boring was continued; at 380 feet a stratum of hard 
rock was encountered, 2 feet thick, and below it a fine stream of water, 
rising, as stated, 3 feet above the surface. The formation at the surface 
is Woods Bluff, and the water supply is from the Nanafalia. 



CONECUH COUNTY. 

Surface Features. 

The older Tertiary formations underlying Conecuh County 
range from the Buhrstone up to the St. Stephens limestone, 
with small tracts of still older beds in the extreme north. There 
is thus a considerable degree of diversity in the topography. 
Overlying the Tertiary beds mentioned, in the southern third 
of the county, is a mantle of the Grand Gulf sands and strat- 
ified clays, and over everything the red loam and pebbles of the 
Lafayette. These two later formations provide as usual, an 
abundance of pure freestone water from shallow wells and 
springs. On the high interstream plateaus, where the Lafay- 
ette mantle is comparatively undisturbed, the wells are of mod- 
erate depth, often less than 50 feet, and along hillsides between 
these plateaus and the stream valleys springs break out every- 
where above the first comparatively impervious layer beneath 
the mantle of sand and pebbles. 



268 DETAILS : COASTAL PLAIN DIVISION. 

Aetesian Prospects. 

While very few deep wells have been reported from this coun- 
ty, there is no reason why borings should not be successful, since 
the Claiborne beds and parts of. the St. Stephens limestone are 
well known to be good artesian reservoirs. Only one well re- 
cord has been obtained. 

EVERGKEEN. 

Town well, in the W. half N. E. quarter Section 3, Township 5, Range 
11; bored by Porter and McDonald in 1903; depth, 168 feet; casing, 6-inch, 
to bottom; water stands at -30 feet; estimated yield by pumping, 115 
gallons per minute; water is pumped into standpipe, from which it is 
distributed through the town. Boring begins in strata of the St. Steph- 
ens, overlain by Grand Gulf and Lafayette; water probably obtained from 
the Claiborne sands below the limestone. 



ESCAMBIA COUNTY. 
Surface Features. 

The surface throughout Escambia County is occupied chief- 
ly by two formations, the Lafayette and Grand Gulf, whose 
sands, loams, clays, and pebble beds' have at one time covered 
all the underlying Tertiary rocks. The Lafayette, here as 
elsewhere, is a mantle averaging 20 to 25 feet in thickness, and 
the Grand Gulf sands and stratified clays are also of the nature 
of a covering formation beneath the Lafayette. The underlying 
Tertiary formations next below the Grand Gulf are the St. 
Stephens or white limestone in the northern part of the county, 
and the sands' and clays of the lower Miocene in the southern 
part. 

The Lafayette and Grand Gulf have been so much eroded 
that they are not now everywhere present, though generally so 
on the higher and more level tracts ; along the slopes and in 
the lowlands they are frequently absent and the Tertiary sands 
and limestones are exposed at the surface. 

The conditions are favorable for shallow waters and a good 
supply may be had almost anywhere in the county from wells 
60 feet or less in depth ; springs also are not rare. 



WATERS OP THE TERTIARY 269 

AKTKSIA \ Pbospects. 

Deep borings for artesian water have as yet been confined to 
the vicinity of the Louisville and Nashville Railroad, mainly 
at Brewton, Harrington, Flomaton, and Atmore, but flowing- 
wells should be obtained by moderately deep borings elsewhere 
in the country where the altitude is not too great. 

BREWTON AND VICINITY. 

Most of the artesian wells in the county are at Brewton and 
in its' immediate vicinity. Mr. W. J. Malone, who has drilled 
very many of these wells', has furnished the following general 
record of the conditions there : 

The shallowest of the flowing wells are only 40 feet deep ; 
the deepest nearly 400 feet. The record in general is as fol- 
lows : surface, sand, gravel, etc., 20 feet; bluish clay, 20 feet; 
just below this in the sands is' the first water. The flow from 
the shallow wells is large at first, but falls off rapidly ; the 
water is strongly chalybeate. 

The sands below the blue marl or clay above noted are 15 
to 20 feet thick, and are followed by 6 feet of white sticky 
mud ; then the second water at a depth of 65 feet, more or less. 
The flow of this is stronger than that of the first, but the water 
is likewise chalybeate. 

The white sticky mud continues 6 feet more, making 12 feet 
in all ; then sand for 5 feet, and a third flow of water at a depth 
of about 75 feet. This water is also chalybeate and the flow is 
a little better than the second. 

Below this are about 100 feet of loose white nonpacking 
sand, then an indurated bed of yellowish limestone 25 to 35 
feet thick, below which, at a depth of about 200 feet, is another 
good flow of water. This is' described as magnesian (lime) 
water, and is quite different from the water obtained above it. 

Below the yellowish limestone are 33 feet of sand, 33 feet 
of blue mud like the first mentioned. 2 feet of very hard dark- 
blue slaty rock, 60 feet of blue clay in egg-shaped lumps, then 
lime rock down as far as the borings have penetrated. In this 
rock the drill will sometimes drop suddenly 2 or 3 feet, as if 
cavities existed in the rock. When the blue mud is' encounter- 
ed, gas nearly always comes up. In the lime rock water is 
obtained in places where the rock is of open texture, or porous. 



270 DETAILS : COASTAL PLAIN DIVISION. 

As before stated, borings have gone into this limestone to a 
depth of about 400 feet from the surface, but the rock has not 
been passed through. The water from this horizon is' decided- 
ly limy, or "magnesian." 

Mr. Malone states that the volume of water from the shal- 
low wells varies with the height of the water in Murder Creek, 
on the terrace of which the town is located, at about 85 feei 
above tide. The shallow wells probably do not go below the 
Grand Gulf beds. ■ 

Among list of the shallow wells bored by Mr. Malone to 
depths of 65 to 80 feet are those of E. Downing (3 wells), 
J. A. McGowan (2 wells'), Jet McGowan, Mrs. Spear, P. B. 
Sowell (2 wells), A. McGowan (2 wells), M. McCall, W. A. 
Harrold, (2 wells), Brewton Gun Club, Phifer's bakery, Pe- 
ters Lumber Company (3 wells), and M. S. Lovelace (2 wells). 
These flow from 2 to 5 gallons per minute, and are generally 
cased for 65 feet with 1 1-4-inch pipe. The. record is practi- 
cally the same for all, as follows : Sands and soil, 0-35 feet ; 
blue marl, 35-45 feet; white sand, 45-65 feet; clay and marl, 
65 feet to bottom. 

Besides these there are about 80 other wells of the same kind 
in and about Brewton with similar records. Among them are 
the Parker well, 68 feet deep; the canning factory well, 75 feet 
deep, with a good flow and water less strongly chalybeate 
than the others from this depth ; Allsup's well, 75 feet deep ; 
2 wells at the ice factory, 42 and 44 feet deep, respectively, 
with strongly chalybeate water. The old McMillan well, bored 
many years ago, has ceased to flow. The water was strongly 
chalybeate. 

The following wells get water from about 175 feet depth : 
Dr. W. H. Malone's, 200 feet deep, but water comes from the 
175-foot level, as the well is on higher ground; Arends Hotel, 
130 feet deep;. Cedar' Creek Mill, 178 feet; Dr. Tarrant's, 175 
feet. These go into the St. Stephens limestone, and all the 
deeper wells are from the same formation. The well at the 
power house has a 2-inch pipe bringing the water from the 
bottom, 393 feet, and an outside 4-mch pipe bringing it from 
the 175-foot level. 

The three following records are of wells recently bored in 
Brewton. 



WATERS OF THE TERTIARY '2 j 1 

Wiley Downing's well, one-half mile from ralroad station; bored by 
David Carpenter in 1904; depth, 509 feet; casing, 3-inch and 2-inch; stood 
at ^21 feet; second water, at 315 feet, overflowed; third water, at 300 
feet; rises 31 feet above the surface; flow. 15 gallons per mniute at 2 feet 
above the surface; water is piped throughout the house and flows a 
strong stream on second floor. 

Record of Wiley Doioning's well, Brewton. 



Feet. 

Sand 0— 12 

Clay 12 — 72 

Sand 72 — ISO 

White lime rock 180 — 216 

Black soft mud (between 290 and 300 feet shell 

embedded in mud) 216 — 300 

Lime rock 300 — 302 

Soft white marl 302 — 315 

Rock 315 — 316 

White soft marl 316 — 328 

Alternating layers of soft marl 10 or 12 feet 

thick and hard rock 3 to 6 inches thick 328 — 509 



E. Downing's well, one-half mile northeast of station; bored by David 
Carpenter in 1904; depth, 360 feet; casing, 3-inch and 2-inch; water rises 34 
feet above the surface; flow, 5 gallons per minute. Record same as ■ 
preceding. 

Cedar Creek Mill Company's well, in the S. E. quarter Section 28, 
Township 2. Range 10; bored by Henry Hammons in 1904; depth, 178 feet; 
casing, iy 2 inch; first water at 50 feet, flowing; second water, at 155 feet, 
flowing one gallon per minute; third water, at 177 feet, flowing 2 gallons 
per minute. Record: Sand and gravel, 0-25 ieet; red clay, 25-30 feet; 
gravel. 30-33 feet; joint clay. 33-45 feet; white marl, 45-55 feet; quicksand; 
55-141 feet; sand and lime rock, 141-17S feet. 

HERRINGTON AND VICINITY. 

J. A. Jernigan's well, Herrington, in the N. W. quarter N. W. quarter 
Section 14. Township 1, Range 9; bored in 1895 by negroes; depth, 117 feet; 
casing, 1% inch to bottom flow, 1 gallon per minute. 

Well at Keego, 1 mile northeast of Herrington, near Louisville and 
Nashville track; bored by negroes in 1902; depth, 135 feet; casing, 1 1-4 
inch, to bottom; original flow, 10 gallons per minute; present flow. 1 gal- 
lon per minute; temperature, 69°. 



The town of Pollard is on the terrace of Conecuh River, 25 
or 30 feet above the bottom lands and perhaps 50 feet above 
low-water level. Many of the wells bored here reach depths 
of 80 to 100 feet, usually less than 90, and are probably alto- 
gether in Grand Gulf strata. They all yield flowing- water 



272 details: coastal tlain division. 

and in most cases good streams, the best of them filling a I 1-2 
inch pipe. Most of the borings' have been made by Charlie 
Sowell, a negro, who gives the following general record : Red 
clay, 0-20 feet ; white sand, 20-30 feet ; white plastic clay, 30-40 
feet; blue sand, 40-55 feet; blue sticky marl, 55-65 feet; at 
about 70-75 feet is usually a streak of black mud, in which the 
water is commonly found; this black mud is just above a blue 
clay. 

Well at Martin Lindsey Hotel, depth, 97 feet; flow, 6 gallons per minute; 
water rises to 7 feet above the surface; temperature, 69°. 

W. A. Findley's well; bored about 1890; depth, 68 feet, (?); casing, 2-inch; 
water rises to 2 feet above the surface; estimated flow, 25 gallons per 
minute; temperature, 69°. 

Lindsey Lumber Company's well; bored by Charlie Sowell; depth, 64 
feet; flow, 7 gallons per minute, water rises to 4 feet above tne surface. 

W. T. Mayo's well, 75 yards south of station; depth, 97 feet; casing, 
V/z inch; flow, 3 gallons per minute; water rises to 3 feet above the sur- 
face; temperature, 69°. 

C. L. Wiggin's well; bored in 1800; depth, 85 feet; flow, 3 gallons per 
minute; water rises to 6 feet above the surface; temperature, 69°; supply 
falls off in dry weather. 

Mat Manning's well; depth, 90 feet (?); flow, 3 gallons per minute; 
water rises to 6 feet above the surface; temperature, 69°. 

B. F. Pringle's well; bored by Charlie Sowell; depth, 104 feet; estimated 
flow, 10 galolns per minute; water rises to 4 feet above the surface; tem- 
perature, 69°. 

I. K. Stubb's well, 400 yards west of station; flow, 3 or 4 ganons per 
minute; water rises to 4 feet above the surface; temperature, 69°. 

M. Lindsey's well; flow, 1 gallon per minute; water rises to 3 feet above 
the surface; temperature, 69°. 

Well at N. N. Martin's turpentine still, one-fourth mile from station; 
bored by Charlie 1 Sowell; depth, 75 or 80 feet; casing, 2-inch; flow, 25 gal- 
lons per minute; water rises to 8 feet above the surface; temperature, 
68%°. 

J. L. Jernighan's well, one-fourth mile west of station; bored by Mr. 
Jernighan; depth, 73 feet; casing, 1V 2 inch; flow, 25 gallons per minute; 
water rises to 3 feet above the surface; temperature, 69°. 

Other wells in Pollard are on Dr. Ford's place; on the Hammock or 
McMillan place, where the stream fills a'1% inch pipe, the temperature of 
the water being 68° ; and at the Bonita Hotel. 

WEST OF POLLAED. 

To the west of Pollard there are few wells and they appear 
to be deeper. At Flomaton, the elevation of which is not 
greatly different from that of Pollard, there is only one well, 
viz, that in Mr. G. A. Ivey's yard. This' well was sunk by driv- 
ing a I i-2-inch pipe with open end down 311 feet, and pump- 
ing out the sand and other materials at intervals through a 



WATERS OF THE TERTIARY 273 

smaller pipe. The water at present (1905) rises 8 or 10 feet 
above the surface, but Mr. Ivey states that when the three 
fourths-inch pipe was in it rose more than 50 feet above the 
surface. The material pumped out was chiefly white sand. At 
211 feet the first water, a powerful stream, was' reached, but 
the sand caved in ana clogged the pipe, and it was not obtained 
again. Mr. Ivey reports that from near the bottom of the well 
was brought up what he thought to be a petrified oak leaf, 
about 3 inches long and narrow like the leaf of the willow oak ; 
he also got at this depth "pieces of charcoal." This statement 
leads to the inference that the boring penetrated the Coal 
Bluff lignite bed, which should be at about this depth here. 
He also reports that; at old Erie (between Pollard and Floma- 
ton) there is or was' a flowing well, in which, at a depth of 
80 feet, a "cypress" log was found. 

A sample of the water from Mr. Ivey's well has been ana- 
lyzed by'Mr. Hodges, with the result given below. 

Analysis of water from G. A. Ivey's well, Flomaton. 



Parts per million. 

Potassium (K) 2.3 

Sodium (Na) 9.2 

Magnesium (Mg) 3.7 

Calcium (Ca) 8.5 

Iron (Fe) 3.8 

Alumina (Al 2 O s ) 2.3 

Chlorine (CI) 2.8 

Sulphuric acid (S0 4 ) 9.4 

Carbonic acid (HCO s ) 64.1 

Silica (Si0 2/ > 15.2 

121.3 



The water has a slight taste of sulphur and stains glasses 
with the deposited iron. 

Further west, at Atmore, in the W. half N. W. quarter Sec- 
tion 29, Township 1, Range 6, a well was bored by W. M. Car- 
,ney in 1902, but no water was obtained and no record is avail- 
able. 



The deepest boring made in Escambia County, is a well 
bored for oil on the banks of Conecuh River 6 miles above 
Roberts. Unfortunately samples of the materials penetrated 
18. 



274 details: coastal plain division. 

at different depths could not be obtained except in a few in- 
stances. At a depth of ioo feet the St. Stephens limestone was 
struck, and the boring was still in the same rock at the depth 
of 190 feet. Claiborne shells were brought up in abundance 
before the drill had gone 700 feet. As nearly as can be determ- 
ined the boring must have gone to the base of the Tertiary, if 
not into the Ripley beds. 

A great volume of water was struck at less than 700 feet. 
It was' estimated that, when half shut off, this flow was 3000 
gallons per minute, and much greater before being reduced. 

The boring was done by M. Canfield in 1902-3. The Grand. 
Gulf sands are at the surface, and the lower part of the river 
bluff is formed by the calcareous sands of Miocene age, while 
the top of the St. Stephens limestone is not far below the water 
level in the river, since it shows in the banks a few miles up- 
stream. The water which pours' out of this well is beautifully 
clear and blue, such as is seen in limestone springs, and is de- 
cided limy. 

The record as given bv Mr. Canfield is as follows: 



Record of well at Roberts. 



Feet. 

Sand — 22 

Blue marl 22 — 37 

Fine white sand 37 — 39 

Gumbo 39 — 60 

Lime rock and shell 60 — Gl% 

Gumbo 61%— 90 

Layers of shell rock and blue clay, 1 or 2 inches thick.. 90 — 90 
Blue clay, 1 foot;' white shell rock, 2% feet; blue clay, 

shell rock, 5 feet; very hard flint rock, 6 in., soft 

lime rock, 2 feet; blue clay, 2 feet 100 — 113 

Lime rock 113 — 120 

Hard lime rock, 18 inches; soft lime rock, 2V 2 ft.; hard 

lime rock, 2 feet 120 — 126 

Lime rock; small slow at about 150 feet 126 — 234 

Lime and sand shale (water) 234 — 248 

Sand rock 248 — 317 

Lime and sand (water) 317 — 337 

Hard sand rock (water ) 337 — 347 

Black muck, green clay, lignite, trace of oil; strong 

flow of water (3,000 gallons per minute) * 347 — 353 

Lime rock, lignite, oily sand 353 — ' 363 

Shale 363 — 365 

Sandy shell rock 365 — 375 

Shell rock 375 . — 388 

*The water from 350 feet came up through a 12-inch pipe 22 feet 

above the ground, then 8 feet through a 4-inch pipe, in all 30 fe*t. 
From the top of this pipe a 4-inch stream was projected 35 feet into 
the air, 65 feet above the ground surface. 



WATERS OF THE TERTIARY 275 

Sandy shale 388 - 401 

Soft, honeycombed lime rock 401 — 413 

Gumbo (sea sediment) 413 — 416 

Hard shell rock 416 — 127 

Soft sand rock, lignite 4i7 — 411 

Lignite 441 — 446 

Sand 44G — 4(56 

Soft lime rock, becoming harder 406 — 480 

Honeycombed lime rock (water) t480 — 490 

Hard lime rock 490 — 505 

Blue marl 505 — 506 

Lime rock 506 — 522 

Soft lime 522 — 524 

Sand, strong flow of water, nearly as great as that at 

350 feet 524 — 526 

Lime rock, sandy at times 526 — 58S 

Sandy shale 58S — 600 

Lime rock, part shells GOO — 629 

Blue sand shale 629 — 639 

Lime rock 639 — 653 

Sand and shale; at 675 feet good flow of water 653 — 698 

Lime rock; thin stratum of coal in last 30 feet 698 — 748 

Shell rock (cap rock) 748 — 75S 

Sand rock, much mica 758 — 764 

Shell rock 764 — 773 

Hard slate 773 — 813 

Shell and lime rock .• 813 — S21 

Sand 821 — 831 

Shell and sand 831 — 911 

Pyrite * 911 — 912 

Blue marl 912 _ — 923 

Gumbo, some shell 923' — 958 

Chalk 9o8 — 960 

Gumbo 960 — 968 

Soft sand rock 9o8 — 988 

Sand rock 988 — t;92 

Pyrite 992 — 9^9 

Gumbo, streaks of shale 99J — 1148 

Dark clay 1148 — llo4 

Hard lime rock, shells Ho4 —1158 

Clay, like lime lioS — Ho9 

Lime, shells, sand rock 1159 — 1164 

Gumbo, some gas 1164 — 1214 

Porous lime rock 1214 — 121.0 

Shale 1220 — 1240 

Soft, porous black rock, oil sand 1240 — 1245 

Dark shale 1245 —1290 

Dark-green sand Lyo — 13< 5 

Soft rock 131.5 — 1310 

Dark shale 1310 —1320 

Gumbo with shell 1320 — 1337 

Soft sand rock 1337 — 1350 

Dark shale 1350 —1355 

Shells, lime rock 1355 — 1360 

Dark shale 13u0 — 1375 

Soft sand rock 1375 — 1380 

Dark shale 1380 — 1390 

White clay 1390 — 14b0 

Soft sand rock, black specks 14oo —1410 

Sandy shale, black specks 1410 — 1422 

Dark shale 1422 —1439 

Pyrites, shells, sand and rock mixed together, salt 

water, flow 150 gallons per minutes 1439 —1484 

Dark shale, hard hard streaks and some shells 1484 — 1522 

Dark clay or gumbo 1522 — 15^0 

Hard flinty rock 1550 — 1553 

Gumbo shale, some shells 1553 —1640 

At this depth the formation should be lower Nanafalia or 

Naheola. At 1300 feet a petrified sea-crab shell was found. 
At 1600 feet, salt water about 200 gallons per minute. 



276 details: coastal plain division. 

MONROE COUNTY. 
Sueface Features. 

The older t Tertiary formations of Monroe County range 
from the Nanafalia sands and marls in the north to the St. 
Stephens limestone in the south, with the capping- formations 
of the Grand Gulf over the limestone and the Lafayette over 
all, where not removed by denudation. This gives the usual 
Coastal Plain variety in the shallow water conditions. Where 
these are dependent on the two capping formations, the quality 
and quantity of the water are generally all that can be desired. 
[n many places', where these mantles have been removed the 
underlying, older Tertiary materials influence the shallow-water 
supply both in quality and quantity. 

Mineral Waters. 

awin and vicinity. 

Near Awin in Wilcox county but across the line in the north - 
eastern part of Monroe county, there is an area in the Nana- 
falia terrane in which are many fine springs. The waters from 
five of these have been analyzed by Mr. Hodges for Messrs. J. 
M. Williams and S. L. Crooks, with results' shown in following 
table. 

Analyses of water from springs in Monroe County near Awin, Wil- 
cox county. 



Parts per million. 
No. 1 No. 2 No. 3 No. 4 No. 5 

Potassium (K) 1.9 

Sodium ,Na) 9.2 

Magnesium (Mg) 1.2 

Calcium (Ca) 13.7 

Iron and alumina (Fe 2 3 , A1 2 3 ) 2.8 

Chlorine (CD 3.5 

Sulphuric acid (S0 4 ) 10.2 

Carbonic acid (HCO s ) 55.7 

Silica (Si0 2 ) 29.6 



Analysis of No. I was made for Mr. J. M. Williams of Awin 
in 1903, the others were made in 1906 for Mr. S. L. Crook and 
others who intended to improve the property with a view to 



1.1 


1.2 


1.3 


.8 


7.7 


7.5 


8.2 


7.0 


4.1 


3.9 


3.2 


4.3 


59.6 


54.1 


36.0 


17.2 


7.3 


1.9 


3.0 


4.8 


6.6 


5.3 


5.3 


3.7 


52.1 


38.2 


23.3 


7.5 


146.4 


148.2 


114.1 


77.7 


49.5 


43.8 


53.9 


31.1 


334.4 


303.1 


248.3 


154.1 



WATERS OF THE TERTIARY 277 

making' it a health resort. The odor of sulphuretted hydrogen 
was noticed when the water No. 5 was examined, but no attempt 
was made to determine the amount since to be of any vaiue 
such determination would have to be made at the spring. 

TUNNEL SPRINGS. 

At about the site of old Kempsville, near the station of Tun- 
nel Springs, on the Louisville and Nashville Railroad, in the 
C. W. quarter S. E. quarter Section 14, Township 8, Range 8, 
are two springs which have lately attracted attention. They 
issue from a high hill of the Buhrstone rock, and are only 
about 15 feet apart. The composition of the dissolved mineral 
matter is similar in the two waters, but with slight differences, 
as' the following analyses by Mr. Hodges will show : 

1 Analyses of water from Tunnel Springs. 



Farts per million. 
No. 1 No. 



Potassium (K) 1.9 1.0 

Sodium (Na) 6.9 4.8 

Magnesium (Mg) 37.4 23.0 

Calcium (Ca) 88. 4 65.0 

Iron (Fe) 44.6 

Iron and alumina (Fe 2 0.,, AU0 3 ) 42.6 

Aluminum (Al) 32.2 

Chlorine (CI) trace trace 

Sulphuric acid (SO4) 618.0 336.0 

Carbonic acid (HC0 3 ) 7.1 

Silica (Si0 2 ) 34.5 39.4 

871.0 511.8 



With this composition these springs should have very de- 
cided medical qualities, but as yet there are no improvements 
or accommodations for visitors. 

Artesian Prospects. 

The Tuscahoma and Nana f alia sands are usually water bear- 
ing and favorable to the success' of artesian borings, and in the 
northern part of the county there should be no difficulty in 
getting artesian water from them. In the southern part the 
Claiborne and St. Stephens formations may usually be counted 
on to yield artesian water. Only two records of deep borings 
have been obtained from Monroe County. 



27S DETAILS : COASTAL PLAIN DIVISION. 

NADAWAH. 

Shoal Creek Lumber Company's well, in the N. W. quarter N. E. 
quarter Section 28, Township 10, Range 9; bored by New Orleans par- 
ties; water stands at -3 feet. 

Record of Shoal Creek Lumber. Company's well, Nadawah. 



Feet. 

Soil 0— 8 

Rock 8— 12 

Soapstone 12 — 30 

Rock 30 — 34 

Soapstone 34 — 48 

Rock 48 — 51 

Soapstone 51 — 59 

Rock 59 — 61 

Sand and shell 61 — 64 

Rock 64 — 69 

Soapstone 69 — 78 

Rock 78— 80 

Sand and shell SO — 90 

Rock 90 — 96 

Saiid and shell 96 — 120 

White sand, with water 120 — 137 

Shell 137 — 156 

Quicksand 156 — 160 

Clay 160 — 168 

Soapstone 168 — 207 

Rock '. 207 — 209 

Soapstone 209 — 259 

Muck 259 — 327 

Black clay 327 — 490 

Shell rock. 4 inches thick — 490 

(?) , 490 — 516 

Rock 516 — 532 

Black clay 532 — 551 

Rock . ; 551 — 557 

Muck 557 — 676 

Rock. S inches thick — 676 

Drab clav 676 — 716 

Rock 716 — 717 

Drab clay 717 — 718 

Rock : 718 — 720 

Black clay 720 — 744 

(?) 744 — 751 

Rock, 18 inches thick 751 — 752 

Drab clav 752 — 781 

Rock 781 — 784 



This record does not give much information as to the strata 
penetrated, but from the depth of the well and its position the 
borings must go into the Ripley sands of the Cretaceous, Nad- 
awah being on the outcrop of the Nanafalia. 

Maros. 

In the lower part of the county at Maros, Mr. J. A. Joullian 
has recently (1906) bored a well for Mr. J. M. Blacksher to 
the depth of 600 feet. 



VVATKRS OF 'I HE TERTIARY 279 

While this boring was a failure as regards artesian water, 
it gives some definite information about the underlying- for- 
mations. The record according to Mr. Joullian is as follows: 

Record of J. M. Blacksher's well at Metros. 



Feet. 

Red clay, gravel and sand — 300 

Hard blue clay or shale 300 — 400 

Sand 4fH» — 4l!0 

Dark In-own clay without fossils A'20 — 460 

Same material more granular in structure. .. .460 — 480 
Same material with small shells of liiio- 

cene age 480 — 500 

Hard blue shale or clay 500 — 540 

Rock 540 — 545 

Blue clay 545 — 585 

Soft blue clay or gumbo 585 — 600 

Hard white limestone rock, bottom of boring.. 600 — 604 



( )n account of the hardness of the rock at the depth of 6oo 
feet and because the upper part of the boring was' not cased 
and getting into bad shape, the drilling was stopped, and an- 
other larger well of io inch diameter, was begun with the in- 
tention of going down to 1500 or 2000 feet depth. At this 
time (Jan. 1907), the boring is down 200 feet in the red clay 
and gravel. 

The shells which were brought up from 480 to 500 feet have 
been identified as being of Chipola age, and the white lime- 
stone is probably either the Chattahoochee limestone of Lang- 
don, or the top of the St. Stephens. 

It is rather remarkable that no water-bearing sands were 
penetrated in the 600 feet of this boring. 



WILCOX COUNTY. 
Surface Features. 

In Wilcox County the older underlying formations' are the 
Ripley in the northwestern part and the lower Tertiary forma- 
tions up to the Woods Bluff and Hatchetigbee in the southern. 
These older formations are covered discontinuously by rem- 
nants of the Lafayette capping of red sandy loams and pebbles. 
In most parts of the county an abundance of good water is 
stored in the superficial deposits' and is recoverable from springs 



280 DETAILS : COASTAL PLAIN DIVISION. 

and wells. Some of the springs are considered to have med- 
icinal qualities, and analyses of the water from two of them 
in the lower part of the county are here presented. 

Mineral Waters, 
caledonia. 

At Caledonia on the land of Mr. W. H. McGraw a well 
about 30 feet deep sunk in materials of the Nanafalia formation 
yields a water with very strong mineral properties, as may be 
seen in the subjoined analysis by Mr. Hodges. 

Analysis of water from well of W. H. McGraw, Caledonia. 



Parts per million. 

Potassium (K) 14.6 

Sodium (Na) 150.6 

Magnesium (Mg) 189. „ 

Calcium (Ca) 649.8 

Iron and alumina- (Fe 2 03, Al 2 O a ) 2.6 

Chlorine (CI) 310.8 

Sulphuric acid (SO4 1712.0 

Carbonic acid (HCO s ) 686.5 

Silica (Si0 2 ) 45.2 

3761.1 



A spring at the foot of a hill close by has also strong as- 
tringent and acid taste. The mineral quality of these waters 
depends undoubtedly on the presence of iron pyrites' in the 
strata. 

SCHUSTER. 

On the property of G. W. Stuart at Schuster are numerous 
springs boiling up through the s'ands on land lying between 
swamp and hills covered with piny woods. The water analyzed 
(by Mr. Hodges) has an exceptionally small amount of dis- 
solved mineral matter, but the relative proportions of the in- 
gredients, i. e., the preponderance of the salts of sodium and 
magnesium, may account for the medicinal qualities. 



WATERS OF THE TERTIARY 281 

Analysis of water from Stuarts Spring, Schuster. 



Parts per million. 

Potassium (K) 1.1 

Sodium (Na) 8.1 

Magnesium (Mg) .7 

Calcium (Ca) .8 

Iron and alumina (Fe<.0 3> A1 2 3 ) .' 1.3 

Chlorine (CI) 3.5 

Sulphuric acid (S0 4 ) 3.4 

Carbonic acid (HC0 3 ) 18.7 

Silica (Si0 2 ) 11.4 

49.0 



On J. M. Williams's' land, on the line between Wilcox and 
Monroe counties, in the N. W. quarter N. W. quarter Section 
22, Township io. Range n, are 12 springs, one of them free- 
stone water, the others mineral. That these springs are in the 
region of the Nanafalia formation is shown by the occurrence 
of rock composed of shells of the characteristic oyster of this 
horizon. As' all of the springs from which the waters have 
been analyzed are just south of the county line and in Monroe, 
these analyses will be found under Monroe county. 

OTHER SPRINGS. 

Between Consul, on the Louisville and Nashville Railroad, 
and Gastonburg, on the Southern Railway is Boiling Springs, 
so-called from the fact that a fine freestone spring boils up 
through the sands. 

Several sulphur springs occur at various points in the county. 
Of these mention may be made of one at Annemanie ; one at 
Pine Hill, on the Southern Railway ; Tait's spring at Blacks 
Bluff, on Alabama River, and one on Judge J. T. Beck's place 
near Camden. 

About Gastonburg and Roberta, in the Cretaceous terranes, 
are small, flat-topped hills capped with sandy strata of the later 
formation (Lafayette). On these hills water is readily obtained 
from shallow wells ; while in the lower lands' near by, lacking 
this capping of sands, there is often a scarcity of water. The 
case is somewhat similar to that of the Forkland country in 
Greene County noticed above, (p. 144.) 



282 details: coastal plain division. 

Artesian Prospects. 

The only deep wells in Wilcox County, records of which 
have been obtained, are those about Pine Hill and Catherine, on 
the Southern Railway ; but there seems' to be no good reason 
why such wells should not be successful in other parts of the 
county, especially in the region where the Nanafalia sands are 
available. The success of the boring at Nadawah, just over the 
line in Monroe County, is indicative of what may be expected in 
the lower part of Wilcox County. 

PINE HILL. 

Well of Vredenburg Saw Mill Co., at Pine Hill, in Section 29, Town- 
ship 12, Range 5 East. Bored by J. H. Wood, of Bristol, Tenn., in 1905. 
Depth, 404 feet; cased to bottom. Plows 3 gallons per minute. 

Altitude of Pine Hill station, 110 feet. 

CATHERINE AND VICINITY. 

The records about Catherine are. as follows: 

Mr. J. S. Robins reports that within 6 miles of Catherine there are 
three wells on his place and his father's old place adjoining on the 
north, all of them about 120 feet deep. At 120 feet quicksand is found and 
the water rises to about -20 feet. In each case a 4-foot well was dug 
down -to water, and buckets are used. The wells are thus little better 
than surface wells, as the water in them is almost entirely sepage water 
except in the dry season. Other surface wells in this vicinity go dry, 
but these furnish water the entire year. 

On the Kirksey place, 4 miles north of west of Catherine is an old 
well, reported to be 300 feet deep, in which water stood at -60 feet; a 
4-foot well was dug around it to the water and buckets were used. This 
is a watering place for a large area in dry seasons. 

On Mr. J. R. Pharr's place, in Catherine, is a dug well 90 to 100 feet 
deep, having 6 or- 8 feet of water in the bottom. It is definitely stated by 
several of the Older citizens that in the bottom of this well is a bored well 
of considerable depth; one report giving it as 800 feet, another as 400 feet. 

Mr. M. A. Boynton, of Catherine, reports several very old wells flowing 
small streams on the north side of i^hilatchee Creek, a few miles north 
and northeast of Rehobeth and AJberta. 

Mr. Dave Vaughn has a 4-foot well 1 mile southwest of Catherine, 15 
feet deep, in the bottom of which is a hole 6 inches in diameter of un- 
known dpth. When the water is dipped out and the well cleaned the 
water rises rapidly and finally stands at -15 feet in dry weather, when 
no seepage water enters. Mr. Vaughn reports several such wells in the 
vicinity. 

All of the above wells probably do not penetrate deeper than the Rip- 
ley formation, which prevails at the surface. 



WATERS OF THE TERTIARY 283 

CLARKE lOUNTY. 
Surface Features. 

The underlying Tertiary strata of Clarke County range from 
from the Tuscahoma or Bells Landing- group up to and includ- 
ing the St. Stephens limestone, but owing- to an uplift of the 
Hatchetigbee anticline, the Jackson anticline, and perhaps 
other disturbances of the strata, there are complications in the 
geologic structure which make its study of exceeding interest 
and which will have to be taken into account in calculating the 
probabilities of success in artesian borings. 

The open, sandy nature of most of these formations and the 
fact that remnants of the great mantle of Lafayette loam and 
pebbles are common on all the great divides insure an abund- 
ance of good* freestone water from springs and open wells in 
nearly every part of the county. 

Mineral Waters. 

As in the adjoining county of Choctaw, the Hatchetigbee 
sands and clays are the source of many springs of mineral 
water, especially sulphur and chalybeate, and along the lower 
border of the Hatchetigbee uplift, of tolerably strong brines. 
While many "salt oozes" spring from the outcrops of Hatche- 
tigbee materials, most of the brines are derived from bored 
wells', and hence they will be considered in connection with the 
artesian prospects. 

TALLAHATTA SPRINGS. 

In Section 26, Township 11. Range 2 E.. are the well-known 
Tallahatta Sulphur Springs, in the lowlands of Tallahatta 
Creek, at the northern base of the Buhrstone hills. These 
springs are very little improved, and the visitors are mainly 
from the immediate vicinity. 

I/)WEE SALT WORKS SULPHUR SPRING. 

This is a fine spring coming like the Tallahatta, from the 
Hatchetigbee clays at the base of a ridge of Buhrstone rocks. 
The water is of a decidedly saline taste, but very palatable. 



284 DETAILS : COASTAL PLAIN DIVISION. 

Other sulphur springs occur with the salt waters of the Hat- 
chetigbee horizon, but they are not improved or visited ex- 
cept by the people living near by. 

Artesian Prospects. 

The water-bearers among the Clarke County strata 
are the Hatchetigbee and the lower Claiborne forma- 
tions, though water may also generally be found in 
tne underlying Tuscahoma sands. Ihe strata in Clarke 
County do not have a uniform southerly dip, but are thrown 
into waves by the Hatchetigbee anticline. This uplift extends 
diagonally through the southern part of the county, but its 
effects are seen throughout the county, especially in the fact 
that by it the St. Stephens limestone is kept as the surface for- 
mation, overlain, of course, by the Lafayette, over two-thirds 
of the entire area. This means that the formations in this' area 
lie nearly flat, or rather in a basin, since the Hatchetigbee sands 
and ciays, after disappearing below the surface above Grove 
Hill, reappear in the vicinity of Tombigbee River at Jackson 
and at other points as far south as Oven Bluff. These reap- 
pearances of the older beds so far south, though in the pro- 
longation of the Hatchetigbee anticline, are due to another an- 
tic.ine, the Jackson. The bearing of these facts on the artesian 
prospects will be evident. 

OLD SALT WELLS. 

Deep borings for water for domestic and similar uses have 
not, so far as information is available, been attempted in Clarke 
County; but many years ago, before or during the civil war, 
on many of the outcrops' of the Hatchetigbee strata, especially 
along the southern border of the Hatchetigbee anticline, and at 
the lower end of the Jackson anticline the occurrence of sak 
springs or oozes in the low grounds of Tombigbee River, both 
in Washington and Clarke counties, led to the boring of wells 
for a more ample supply of brine for salt making, and there 
are scores of these old wells in both counties', bored to depths 
varying from a few feet to 400 feet as a maximum. All of them 
overflow, being located as a rule in the palmetto flats of the 
creeks such as Stave, Jackson, and Salt creeks, usually near 



WATERS OF Tin; TERTIARY 285 

their mouths but occasionally 2 miles or more from the river. 
Some of the salt wells are merely excavations around the salt 
oozes, filled to the brim with the brine. During the war these 
places were centers of salt production for the State and for 
the Confederacy, the men engaged in the manufacture being 
exempted from military, duty. The principal production was 
at the Upper, Middle, and Lower Salt Works, the first being 
in T. 7, Range 1 E., the second in Township 6, Range 2 E., 
and the last in Township 5, Range 2 E., not far from Oven 
Bluff. The Upper Salt Works, and the lower works, near 
Oven Bluff, have been patented to the State of Alabama, 
under the names "salt reserve lands." 

A small amount of natural gas comes with the salt water 
from these wells in most cases, and at some of them especially 
where the brines" are weak, there is a good deal of sulphuretted 
hydrogen. 

In the low grounds' of Bassetts Creek, south of Jackson, is a 
bored well, 105 to no feet in depth (presumably altogether in 
the Hatchetigbee formation), which yields a good stream of 
sulphur water, rather strongly impregnated with salt. This is 
one of the most agreeable to the taste of any of the si^phur wa- 
ters of the State, and it has recently been piped a few hundred 
yards from the well up to a pavilion at the railroad station 
in the northwest corner of the S. W. quarter N. E. quarter 
Section 9, Township 6, Range 2, where it comes up through 
a marble vase provided for it. (PI. XVII, B.) The compo- 
sition is shown by Mr. Hodges' analysis below : 

Analysis of water from well on Bassetts Creek, near Jackson. 



Parts per million. 

Lithium (Li) trace 

Potassium (K) 8.2 

Sodium (Na) 960.3 

Magnesium (Mg) 16.0 

Calcium (Ca) 5-1.0 

Iron and alumina (Fe 2 O s , A1 2 3 ) 2.6 

Chlorine (CD 1466.5 

Sulphuric acid (SO4) 6.4 

Sulphuretted hydrogen (H 2 S) * 

Carbonic acid (HCO s ) 267.1 

Silica (Si0 2 ) 17. S 

279S.9 
♦Present not determined. 



286 DETAILS : COAST vL PLAIN DIVISION. 

The bored well which furnishes this water is very near the 
center of Section 9, Township 6, Range 2, and a few yards 
southwest of it is another well, the Saint well, which yields 
a sulphur water with less salt than the Jackson well. In the 
northwest quarter of this section, about 100 yards" west of the 
pavilion, or vase of the sulphur well, is another bored well 
yielding- a chalybeate water, like the others somewhat impreg- 
nated with sulphur. A fourth well is in the low grounds of 
the creek, about a mile west of the wells here described. In 
all these wells the water overflows. 

About 5 miles above Jackson, at Glendon station, on the 
Southern Railway, there is a flowing well bored eight or ten 
years ago by Mr. Welch, then in charge of the sawmills at that 
place. 

Two miles beyond Glendon, at Walker Springs, there are 
three old wells sunk before the war. One of these, south of 
the railroad, is near the site of the old hotel and constitutes the 
springs from which the place is named. The other two are 
nearer the railroad. A fourth well was' sunk by Mr. Savage 
about ten years ago at his store near the railroad. All these 
wells overflow. 

RECENT BORINGS. 

The discovery of oil at Beaumont, Tex., a few years ago led 
to the search for oil in many parts of the South and the brine 
and gas wells of Clarke and Washington counties naturally 
attracted attention with the result that drilling was soon begun 
in all the old salt-works regions. A few of the records of these 
borings are here given through the courtesy of Messrs. S. A. 
Hobson and W. R. Osborne, In many cases the records were 
not accurately kept, and only scanty notes, mainly of the depth 
of the borings and the depths at which water was encountered, 
are now obtainable 

Well at Beckham's Landing, near McGrew Shoals; bored in 1903-4; depth, 
2600 feet, 

Bolen well, in the northeast corner of the S. E. quarter S. E. quarter 
Section 17, Township 7, Range 1, E.; bored under the direction of S. A. 
Hobson in 1902-3. 



WATERS OF THE TERTIARY 287 

Record of Bolen well. 



40 
1 


CO 
61 


3 


04 


40 
25 


104 
129 


.00 
10 


229 
239 



Material. Thickness. Depth. 

Feet. Feet. 

Lafayette loam with gravel at bottom 20 20 

Dark-blue and greenish marl and sanely clays, 

with occasional pyrite nodules 

Ledge of rock (strong gas flow just below this) 
Indurated sand rock (more gas and undetermin- 
ed volume of salt water) 

Dark marls with pyrite nodules interspersed 

(more gas and film of oil)) 

Quicksand, with lignitic streaks near bottom 
Dark marls and clays, occasionally slightly 

sandy 

Light-colored, slightly indurated sand rock 

Dark gummy clays or marls, exuding a black, 
molasses like odorless fluid, which fluor- 
esces in certain lights 90 329 

Alternations of dark gummy shales, sand clays, 
and clayey sands, with occasional pyrite 
nodules (gummy shales aggregating 90 

per cent, of the mass) 377 706 

Hard, almost quartz-like sand rock 4 710 

Loose sands, dark-colored gray grains, full of 
fish remains (strong stream of salt water 
—about 6 per cent, solution— with gas 
that burns steady flame 15 inches high 
from mouth of 6-inch pipe) 30 740 



At 740 feet the Bolen well was discontinued, owing to inabil- 
ity of the contractor to complete his contract The strata of 
the Buhrstone occupy the surface at the mouth of the well. 
with the St. Stephens limestone on the elevations near by. At 
740 feet the boring would probably reach the Manafalia sands. 

A sample of the brine from an old well close to the Bolen 
well has been analyzed by Mr. Hodges. This brine was used 
during the civil war in the manufacture of salt, and may be 
taken as 1 a fair representative of that class of water. 

Analysis of water from old salt well near Bolen well. 



Parts per million. 

Pos+assium (K) 144.0 

Sodium (Na) 11472.0 

Magnesium (Mg) 122.4 

Calcium (Ca) 246.8 

Iron and alumina (Fe-O.v ALO3) 5.2 

Chlorine (CD 18520.0 

Sulphuric acid ( q O.) trace 

Cnrbonie acid (HCO,) 26.1 

Silica (Si0 2 ) 8.2 

30544 7 



288 



DETAILS : COASTAL PLAIN DIVISION. 



Edgar well, on Bumpus land, in the N. W. quarter S. W. quarter Sec- 
tion -6, Township 7, Range 1 E.; drilled by W. R. Osborne, of Mecuchen, 
N. J., for the Edgar Oil Company in 1903-4. 

The following record was furnished by Mr. Osborne: 

Record of Edgar well. 



Material. Thickness. Depth. 

Feet. Feet. 

Sand 10 10 

Limestone 4 14 

Mud 3 17 

White chimney rock (St. Stephens limestone).. 83 100 

Yellow sand, dry 10 110 

Blue sandy clay 5 115 

White limestone 50 165 

Sand 20 185 

Shells 5 190 

Black clay 25 215 

Black sand 10 225 

Gray sand and shells 50 275 

Buhrstone 47 322 

Clay with mica 2 324 

Sand and shells (slight show of oil) 28 352 

Bluish sand 28 370 

Buhrstone and shale 32 402 

Coarse water-sand 55 457 

Green clay and stone 47 504 

Green clay and stone, showing oil and gas 24 528 

Gumbo 37 565 

Gray and black sand 5 570 

Light-colored gumbo, turning dark 132 702 

Black sand and shell, with gas and oil 2 704 

Black gumbo 1 705 

Gray sand and clays,' with gas 120 825 

Gumbo 80 P05 

Sand, with water and gas 25 930' 

Blue gumbo 30 960 

Sand and gas 15 975 

Blue gumbo 5 980 

White clay 2 982 

Very black sand 1 983 

Gumbo 52 1035 

Sand 20 1055 

Gumbo 47 1102 

Black sand and gas 6 1108 

Light-colored clay 52 1160 

Gumbo (stopped on rock) 41 1201 



This boring beginning at the St. Stephens limestone, which is passed 
at 165 feet, probably goes into the Naheola beds. 

Bush well, on State Salt Reserve lands, (Upper Salt Works) half a 
mile northwest of the Edgar well, in the center of Section 27, Township 
7, Range 1 E.; bored by George O. and W. R. Osborne for T. G. Bush 
& Co., in 1902; record not obtained. 

Salt Mountain well, in the southwest corner of the N.- W. quarter S. 
W. quarter, Section 34, Township 6, Range 2 E.; bored in 1904-5 under the 
direction of S. A. Hobson. 



WATERS OF THE TERTIARY 289 

Record of Salt Mountain well. 



Material. Thickness. Depth. 

Feet. Feet. 

Surface soil and clayey sand 7 7 

Bluish clay 10 17 

Fossiliferous limestone ledge % 17% 

Gravel (strong stream of salt water, some gas) 2 19% 
Dark-greenish, unctious-feeling, acid-tasting 
substance containing occasional fossil 
shells or prints, weathering white on ex- 
posure to air 2 21% 

Gravel and clear sand 49 70% 

Indurated dark-grayish sand rock 4 74% 

Dark-gray sand, partially indurated, with oc- 
casional very hard ledges 50 124% 

Dark gummy shale, exuding odorless, molasses- 
like scum; very compact formation as a 
whole, but with thin streak of gravel and 
sand: nodules of pyrite interspersed 

throughout 215 339% 

Indurated ledge of sand rock 1% 341 

Gummy shale similar to that 215 feet 100 441 

Very hard conglomerate; sand, gravel, pyrites 

and ocasional shell fragments 5 446 

Gummy shales with many pyrite nodules and 
occasional shale "pots" which cave under 

water pressure 75 521 

Mixture of clay, gravel, and shells, capped 

with indurated ledge 12 533 

Gummy clays, with occasional alternations of 

siliceous shale and pyrite nodules 196 729 

Compact shale ledge 1% 730% 

Sand, almost hard enough to make self-sus- 
taining walls 77% 808 

Very hard ledge, semi-crystalline sand rock 1 809 

Partially indurated sand 92 901 

Peculiar dark sandy shale, somewhat shot 
shaped when wet but rather amorphous 
when dry, pouring out of hole in volumes 
as drilling progressed 20 921 



At this depth the boring beginning near the top of the Hat- 
chetigbee would probably be down into the Nanafalia or thr 
Naheola. 



19 



290 details: coastal plain division. 

CHOCTAW COUNTY. 
Surface Features. 

The strata of the entire Tertiary series, from the Sucarno- 
chee up to the St. Stephens limestone, are involved in the struc- 
ture of Choctaw County ; and in addition to this, in the south- 
ern part of the county an anticlinal uplift brings up the Hatche- 
tigbee clays in the midst of the St. Stephens territory. Rem- 
nants of the Lafayete sands, loams, and pebbles are found 
capping some of the divides and forming as usual level pla- 
teaus. Under these conditions there is no lack of good water 
from springs and open wells. 

Mineral Springs. 

Waters of medicinal quality are furnished by a number of 
formations in this county — the Claiborne, Hatchetigbee, Woods 
Bluff, Tuscahoma, Nanafalia, and Naheola — practically the 
whole series occurring in the county. A rather full list of 
these springs is here presented through the courtesy of Mr. O. 
C. Ulmer, of Butler. 

Springs of the Claiborne formation. 

THORNTON SPRINGS. 

On Surveyors Creek, in the S. E. quarter N. E. quarter Sec- 
tion 24, Township 11, Range 3 W., there are two or three 
strong sulphur springs which were thought by some to be equal 
to the Bladon Springs. Before the War this was a noted re- 
sort ; it is now practically disused. 

mineral extracts. 

In this connection it may be proper to notice certain min- 
eral extracts which have been put on the market and have had 
considerable sale because of their medicinal value. One of 
the first of these to come into notice was the "Extract of acid 
Iron earth." This was made from the dark-colored, carbo- 
naceous, sandy, pyritous clays of the Claiborne formation near 
Bladon Springs, by drying the clay under shelter for some 



WATERS OE THE TERTIARY 291 

time, during which, by the oxidation of the pyrite and the ac- 
tion of the decomposing vegetable matter, sulphates of iron, 
alumina, and other bases, were formed, impregnating the 
earthy matter. The teachings of this, with as nearly as pos- 
sible uniform concentration, were put up into bottles and placed 
on the market. 

In the vicinity of Fail, in the .same county, a similar "Min- 
eral extract" has been made from pyritous, carbonaceous clays 
of the Claiborne formation. 

Of late the ''Extract of acid Iron earth," evaporated to dry- 
ness and the solid residue pressed into tablets, has been sold 
under the name of Natona. 

Springs of the Buhrstone and Hatchetigbee formations. 

The Hatchetigbee anticline brings to the. surface, in the 
southern part of Choctaw county, a narrow strip of Hatche- 
tigbee clays surrounded by the materials of the Buhrstone, all 
having a northwest-southeast trend. In this area in Choctaw 
and the adjoining parts of Washington County are mineral 
springs, gas springs, and salt well almost innumerable. Only a 
few of the best known can be mentioned. 

BLADON SPRINGS. 

The most important of the springs of the Hatchetigbee are 
the Bladon Springs, embracing a number of springs which 
yield different kinds of water — sulphur, soda, vichy, etc. The 
chief of these is the Bladon Spring, of sulphur water, in the ex- 
treme northeast corner, of the S. E. quarter Section 20, Town- 
ship 9, Range 2 W. A few yards away, in the southeast corner 
of the northeast quarter of the section, is the vichy spring, close 
to the line between sections 20 and 21 ; the grounds of the 
springs include parts of both sections. 

No recent analyses of the waters from these springs are 
available, but the following, made many years ago, are taken 
from Crook's "Mineral Waters of the United States and their 
Therapeutic Uses," page 86, and are presented in their original 
form. 



•292 details: coastal plain division. 

Analyses of Waters from Springs at Bladon Springs, Choctaw County. 



One U. S. Gallon 
contains; 



Solids. 



Sodium carbonate 

Magnesium carbonate 
Calcium carbonate .. 

Iron carbonate 

Calcium sulphate 

Iron sulphate 

Sodium chloride 

Strontia 

Silica 

Organic matter 

Crenic acid 

Hypocrenic acid 



Total 



Gases 



Carbonic acid , 

Sulphuretted hydrogen 
Chlorine , 



ft 


ft 


ft 




£ 


£ 


£ 




to cat- 


r! cH~h- 


b oS-; 


>> 


chy 

ring 

L. 

ddel 


ancl 

ring 

L. 

ddel 


lphi. 
ring 
L. , 
ddel 


to -9 

■Hft'S 


>««£ 


fflmftft 


2 ft/J'/O 


•- 1 ft : ^ 

omrtfq 


46.33 


41.21 


34.93 


32. 89 





29 . 


0.61 


0.65 


1.36 





87 


2.14 


2.42 


2.75 





49 " 


0.23 


0.76 


0.02 


2 


25 


2.79 


2.96 


6 ."24 
7.69 

0.32 
2.10 


2 


26 


1.90 


1.25 


6.75 

O.'iO 


52.49 


48.88 


42.97 


48.72 


Cubic 


Cubic 


Cubic 


Cubic 


inches. 


inches. 


inches. 


inches. 


65.44 


59.20 


52.88 
0.56 


32.56 


1.S4 


1.84 


1.84 





Total 



67.28 



61.04 



55.28 



While these analyses as thus stated, do not accord altogether 
with modern views, they possess a certain historic interest and 
.show very clearly the character of the waters as being alka- 
line carbonated with predominance of sodium ; one containing 
also sulphuretted hydrogen. 

Plate XXIV shows the Hotel and the pavilion over the sul- 
phur springs at Bladon. 

Between Bladon and Cullom, in the S. E. quarter of Sec- 
tion 20, Township 9, Range 2 W., a strong chalybeate spring 
issues from below a bluff of Hatechetigbee clays. South of 
the stores and post-office at Bladon there was formerly an 
alum spring and close by an alum well, both being now dis- 
used and filled up. 

About one mile from Bladon, in the northwest corner of 
Section 29, Township 8, Range 2 West, are the Cullom springs 
with similar variety of waters. Plate XXV shows the Hotel at 
Cullom Springs. , 



GEOLOGICAL SURVEY nl ALABAMA. 1 N lll-:U( , ROIN I) WATKK l(l:Sm'KCi:S. I'l.ATK XXIV, 




A. Hotel at Bladon Springs, Choctaw County. 




Pavilion of Sulphur Spring, Bladon Springs, Choctaw Counti 



WATERS OK THE TERTIARY 293' 

Bladon was a noted resort before the war for the people 
of Mobile and New Orleans. At present, although both Bla 

don and Cullom are well fitted for the accommodation of 
guests, the number of visitors is relatively small because of 
the irregularity in the running" of the boats and the distance 
from railroad lines. 

SPRINGS ALONG TURKEY CREEK. 

In other parts of the Hatchetigbee outcrop, and in the sur- 
rounding Buhrstone northwest of Bladon and particularly 
along the several branches of Turkey Creek, mineral springs, 
gas seeps, and sticks or licks are numerous and characteristic. 
Carbonate of soda seems to be a very constant ingredient of 
the waters, whether sulphur and other mineral ingredients are 
present or not. Where these soda springs come up in the 
creek flats, a crust is sometimes formed which is firm enough 
to walk on ; but fissures and cracks soon develop, the crust 
breaks up, and a black or dark-colored mud, of the consistency 
of mush, oozes out. These places are devoid of vegetation and 
during dry weather become covered by an efflorescence of car- 
bonate of soda, according to general belief, though no analysis 
has as yet been made of it. This deposit is extremely attract- 
ive to cattle and deer and thus gives rise to the common name 
"licks," or "sucks." It is often necessary to fence in the licks 
to prevent loss of cattle by miring down in the semi-liquid mud. 

Dansby Springs, in the N. E. quarter Section 6, Township 9, 
Range 2 W., is a collection of iron, sulphur, and soda springs 
and sucks. At Zeb Taylor's in Section 14, Township 9, Range 
3 \Y., is a strong sulphur spring; and at Zack Rogers's, in Sec- 
tion 34, Township 9, Range 3 W., is a strong chalbeate spring, 
near Conner's Natona bed above referred to (p. 291). Ail 
these are on Turkey Creek and along the axis of the Hatche- 
tigbee anticline. 

OTHER SPRINGS. 

Further north, in its regular place, the Hatchetigbee is again 
the source of mineral springs, of which the following may be 
noted : 

Chapman Springs, in the southeast corner of the S. W. quar- 
ter Section 36, Township 13, Range 3 W., about 3 miles south- 



294 DETAILS : COASTAL PLAIN DIVISION. 

west of Butler ; strongly chalybeate water ; no improvements. 

Walker Spring, in the S. W. quarter N. E. quarter Section 
25, Township 13, Range 3 W., 1% miles southwest of Butler; 
fine chalybeate spring; no improvements. 

Another spring, in the S. E. quarter N. W. quarter Section 
14, Township 13, Range 3 W., 'is not now used. 



Springs of the Woods Bluff formation. 
Butler and vicinity. 

In the valley of Wahalock Creek, near Butler, are several 
fine springs of sulphur and chalybeate waters, locally well 
known, but without accommodations for guests. 

Scarlock Springs, in the S. W. quarter Section 2, Township 
12, Range 2 W. ; chalpbeate water, a bold stream. 

Jackson Mineral Spring, in the N. W. quarter S. E. quar- 
ter Section 4, Township 13, Range 2 W. ; white sulphur; a 
strong flow. 

Chalybeate Spring, in the S. W. Section 3, Township 12, 
Range 2 W., near the bridge over Wahalock Creek ; has strong 
taste also of sulphur. 

Spangenburg Iron Spring, in the city of Butler ; also issues 
from the Hatchetigbee. 

At Pushmataha, a few hundred yards north of the negro 
church, there is a bold chalybeate spring in the edge of a 
branch. The water rises in the "gum" about 2 feet above the 
general surface. 

Springs of the Tnscahoma formation. 

Eureka or Sharon Springs in Section 33, Township 15, 
Range 3 W. ; white sulphur. 

Springs of the Nanafalia formation. 

Rutledge Spring, in Section 15, Township 15, Range 3 W. ; 

On the J. A. Watters place, half a mile below Gays Landing, 
on the Choctaw County side, a great volume of blue water 
rushes out in the edge of the river and the clear stream can 



WATERS 01* THE TERTIARY Zuo 

be traced for a long distance sharply defined against the gen- 
erally turbid river water. This stream issues from the Nana- 
falia marl beds which there form the hanks of the river. 

Springs of the Naheola formation. 

Ashford Springs, in the E. half S. W. quarter Section 15, 
Township 15, Range 2 W. ; once celebrated resort for the 
wealthy planters of Sumter and Choctaw counties ; now in de- 
cay, with nothing to mark the former importance of the place 
except the marble basin of the spring. One of the springs 
here is a white sulphur, one a sulphur-chalybeate and one 
a vichy. 

Artesian Prospects. 

While the number of artesian wells in Choctaw County may 
be counted on the fingers of one hand, success should follow 
deep borings in almost every part of the county. This is ren- 
dered practically certain by the experience in the adjoining 
county in Mississippi, where there are many artesian wells ob- 
taining their water in the Hatchetigbee sands and the lower 
Claiborne beds. 

CULLOM SPRINGS. 

The most instructive boring made in Choctaw County is at 
Cullom Springs, near Bladon. This was started in 1881 and 
finished in 1885 by Captain Trowbridge who was seeking pe- 
troleum. The surface rocks are probably the uppermost strata 
of the Hatchetigbee. The boring penetrated the underlying 
Tertiary beds and the Ripley and, as the record is interpreted, 
about 125 feet into the Selma chalk. While it is impossible 
to identify with certainty the beds penetrated by this boring, 
yet there are several points which seem to be pretty well de- 
termined. Thus in the lower part of the boring the black or 
dark-blue clavs of the Sucarnochee seem to be unmistakably 
shown as well as the clayey sands with shells' of the Ripley 
and the 125 feet of uniform blue rock of the Selma chalk at 
the base. 

The whole depth of the boring is 1345 feet and the record 
obtained from Captain Trowbridge is as follows : 



296 DETAILS : COASTAL PLAIN DIVISION. 

Record of Cullom Springs boring. 



Material. Thickness. Depth. 

Feet, b eet. 
Loose surface materials, varying- slightly in color and texture 80 .SO 

Alternations of blue and sandy marl (clay), with indurated 

blue ledge 5 feet thick at base 81 161 

Soft clayey marl 23 184 

Greensand, with shells, 3 feet, followed by 22 feet alternating 

hard and soft beds, the latter fossiliferous and water 

bearing 25 £09 

Marls or blue clays 46 2o5 

Brown and blue marls (clavs) in many alternations (lignitic ?) . . 21 2Y5 

Blue marls or clays, with 2 feet of greensand at base 61 337 

Lignite, 5 feet, followed by 19 feet of brown, tough marl (clay) 24 361 

Blue sandy marl, with many varieties of shells; Venericardia 

planicosta recognized 23 384 

BIui.-. sandy marl (clay) 58 442 

Brown marl (clay), 5 feet, with 32 feet blue marl below 37 479 

Greensand marl, 9 feet, followed by 37 feet of blue marl (clay); 

at 500 feet water was struck, which flowed 10 feet above 

the surface 46 525 

Brown clay marl, 19 feet, followed by 15 feet of blue clay with 

greensand, containing shells 34 559 

Brown marl, resembling soapstone; contains shells; stream of 

water near bottom which flowed 30 feet above surface 50 609 

Gray sandy marl, with shells 15 624 

Gray sandy marl, with shells; more clayey than preceding 64 688 

Very tough blue marl (clay), at base of which is a thin layer 

of white sand and then a thin layer of greensand 71 759 

Brown marl (clay), 5 feet, followed by alternating beds of 

clay and sand, mostly sand (first salt water) 20 779 

Alternations of gray and brown sand, with marl (clay) 26 805 

Tough blue marl (big vein of salt water) 13 818 

Sand and clay alternating 14 832 

A kind of white limestone (?) containing mica, passing below 

into 3 feet of blue sandy marl, containing shells 28 860 

Blue marl (Clay), 14 feet, followed by 14 feet of blue marl 

and sand, numerous shells 28 888 

Marl 12 feet, with streaks of sand, followed bv brown sand and 

marl, 12 feet 24 912 

Greenish rock, chalky above, hard below 11 923 

Sandstone, 4 feet, followed by 25 feet of white, blue, and gray 

quicksand (strong stream of salt water) 29 952 

Marls or clays, mostly grayish or light brown, with several 

ledges of extremely hard rock, e. g, one 2 feet thick at 

966 feet, one 1 foot thick at 971 feet, one 3 inches thick 

at 978 feet, one J. foot thick at 1000 feet 137 1089 

Tough black clay, 2 feet, followed by 99 feet of dark blue clay, 

some of it quite hard and firm, some very soft and 

sticky 101 1190 

Snuff-colored clay, soft and sticky 13 1203 

Gray sand and shells, 12 feet, followed by 5 feet of soft sandy 

clay 17 1220 

Hard ledge, 4 inches thick at top. below which are about 

125 feet of moderately hard grayish or blue rock, Wn.h 

scarcely any change in color or texture, to oottom of 

boring; no shells observed; "Rotten limestone" 125 1345 



The following additional notes regarding this well may be 
of interest: At 80 feet water was struck, but it did not over- 
flow. At 200 feet there was a bold stream of mineral (vichy) 
water, which overflowed. At 400 feet another strong stream 
of mineral water, like the preceding. At 1,000 feet a stream 



WATERS OF THE TERTIARY 297 

of salt water with inflammable gas was struck. The present 
flow combines the streams at 200, 400, and 1,000 feet. The 
water is decidedly salty, and has a temperature of 83°. The 
gas collects in hubbies or in a foam on the surface of the water 
in the tank into which the stream flows. A lighted match 
touched to this foam ignites the gas, which burns over the 
surface of the water for some minutes, unless extinguished by 
accidental splash. The gas may also be ignited at the spout, 
where it burns with a flame 6 or 8 inches high. The estimated 
flow is 10 to 15 gallons per minute. Plate XXVI shows the 
house enclosing this well and through the open door the stream 
may be discerned. The quality of the water is shown in the 
accompanying analysis, by Air. Hodges : 

Analysis of CulJom Springs water. 



Parts per million. 

Potassium (K) 21.0 

Sodium (Na) 4043.0 

Magnesium (Mg) 35.3 

Calcium (Ca) 74.9 

Iron and alumina (Pe : 3 , A1 2 3 ) 3.8 

Chlorine (CI) 6098.9 

Sulphuric acid (SOi) trace 

Carbonic acid (HCO a ) 457.5 

Silica (Si0 2 ) 9.9 

10744.3 



Well in court-house yard, depth, 600 feet ; water stands at 
-30 feet ; temperature, 77°. No record obtainable. Butler is 
on the Woods Bluff formation, and at the depth of 000 feet 
the boring is probably in the Xaheola sands, or possibly no 
deeper than the Nanafalia. 



"IV ASH IX G TON GO ( XTY. 
Surface Features. 

In the northeast corner of Washington County, by reason 
of the anticlinal uplift already mentioned under Choctaw 
County, the Tertiary strata down to the Hatchetigbee are 
brought to the surface. In the rest of the county the only 



298 DETAILS: coastal llain division. 

Eocene formation occurring at the surface is the St. Stephens 
limestone. Over the greater part of the territory of the latter 
is spread a later formation, the Grand Gulf, which, together 
with the Lafayette, is responsible for the soils and much of 
the topography, and in still greater degree for the shallow 
waters. Where the loams and sands of the Lafayette are the 
surface materials there is always an abundant supply of the 
very best water in springs and open wells. Where the lime- 
stone is the surface formation the water conditions are not so 
favorable, but it must be remarked that in most of the St. 
Stephens area the two capping formations are present. 

Mineral Springs. 
Springs in the Hatchetigbee formation. 

The outcrop of Hatchetigbee clays and sands, with their in- 
closing Buhrs'tone strata, caused by the anticlinal uplift, is the 
source of numerous mineral springs in Washington county, as 
it is in Choctaw County adjoining. 

The salt springs or oozes will be more particularly described 
below in connection with the artesian borings made in search 
of brine for salt manufacture. The other mineral springs of 
the Hatchetigbee anticline comprise sulphur, soda, and iron 
waters, in most of which there is more or less natural gas. 

In the palmetto flats of an affluent of Santa Bogue Creek, 
in the N. W. quarter N. E. quarter Section 9, Township 8, 
Range 2 W., is Sanderson's spring, at which there has been a 
slight effort at improvement by providing a box. The water 
here has a soft, alkaline taste, with a suspicion of sulphur. In 
the sloughs or abandoned channels of the creek near by are 
many other similar springs, not at all improved but of a de- 
cided mineral character. In all of them bubbles of natural gas 
are constantly rising. Higher up the creek, at John Long's 
place in the S. W. quarter Section 6, Township 8, Range 2 W., 
there is a mineral spring similar to the vichy spring at Cul- 
lom, said to contain carbonate of soda and some sulphur. 

Farther down, near Santa Bogue, is Salt Pond, formerly a 
beaver pond, receiving the streams from several salt wells in 
the vicinity. The dam has been cut and the pond drained 
away, and the place is now of the nature of a suck or lick, a 



GEOLOGICAL SURVEY OF ALABAMA. UNDKKGKOl'N'l) WATER RESOURCES, PLATE XXVII. 




A. Mound Spring at Healing Springs, Washington County. 




B. Creek Spring at Healing Springs, Washington County 



WATERS OF THE TERTIARY 299 

spot bare of vegetation, an acre or two in extent, and covered 
in dry weather, according to popular belief, by an efflorescence 
of carbonate of soda. In the midst of this area there seems to 
be an ooze of soft or semiliquid mud of black or dark color, 
over which at times a crust forms that is firm enough to bear 
the weight of a man, but trembles under foot. Cracks and fis- 
sures gradually develop in this crust and it breaks up, letting 
out the black mud. Cattle and deer are fond of the soda salt 
that accumulates on the surface of these sucks and it is nec- 
essary to fence them in, as the cattle mire down in them. 

As in Choctaw County, carbonate of soda seems to be a 
characteristic ingredient of the mineral waters of the Hatche- 
tigbee anticline, whether or not sulphur and iron are also 
present. 

Springs of the Grand Gulf formation. 

The Grand Gulf formation in most of the region of its oc- 
currence, both in Mississippi and Alabama, is the source of nu- 
merous mineral springs, especially of such as are charged with 
the salts of magnesium and with iron. The percentage of these 
dissolved salts is often small, however, as may be seen from 
the analyses given below. 

HEALING SPRINGS. 

In the northwestern part of the county, near the inland mar- 
gin of the Grand Gulf formation, are the Healing Springs, 
on a branch of Santa Bogue Creek. The springs, 17 in num- 
ber, occur m the low grounds and marshy spots along the 
stream. The water is under a slight hydrostatic pressure 
which causes it to rise a few feet above the general level of 
the stream when confined by boxing or by pipes. The water 
is remarkably clear and pleasant to the taste ; it contains a small 
proportion of dissolved solids, but these are in combinations 
which probably give them their therapeutic value. The analy- 
ses of the water from four of the springs, by Mr. Hodges, will 
show clearly the nature of the water. The situation of the 
springs, in the midst of a forest of yellow pine, is a distinct ad- 
vantage to the seeker for health. 



300 DETAILS: COASTAL PLAIN DIVISION. 

Analyses of Healing Springs waters. 



Potassium (K) 1.6 

Sodium (Na) 2.2 

Magnesium (Mg) 1.9 

Calcium (Ca) 8.5 

Iron and alumina (Pe 3 3 , A1 S 3 ) 4.9 

Chlorine (CI) 3.5 

Sulphuric acid (SO t ) 11.5 

Carbonic acid (HC0 3 ) 23.3 

Silica (Si0 2 ) 28.8 



Parts per million. 
No. 1 



No. 1 


No. 3 


No. 4 


1.5 


1.9 


1.9 


2.6 


3.4 


2.3 


2.0 


1.9 


1.4 


9.2 


S.l 


5.2 


4.9 


5.5 


4.1 


3.5 


3.5 


3.0 


8.9 


9.8 


9.6 


31.7 


29.3 


13.8 


27.1 


29.1 


26.6 



No. 1. Mound Spring. 

No. 2. Creek Spring. 

No. 3. Scholes Spring. 

No. 4. McCartney Spring. 



86.2 91.4 92.5 



Artesian Prospects, 
old salt wells. 

Within the area of the St. Stephens limestone, and especially 
along the southern border of the Hatchetigbee auticline, a very 
large number of borings have been made, most of them before 
the civil war, for the purpose of obtaining brine for the manu- 
facture of salt. These salt wells are most abundant in Wash- 
ington County in the palmetto flats bordering Salt Creek and 
the tributaries of Tauler Creek, generally within a mile from 
Tombigbee River and in a strip extending nearly parallel with 
its course from a mile or two above old St. Stephens nearly to 
Frankville. The wells have been bored to depths varying from 
150 to 400 feet, and in one instance the depth has been given as 
800 feet, in the case of a well at the Morgan Salt Works. At 
the Bucksnort Salt Works, near Peevy's Landing, according 
to Mr. Coleman, the deepest well was 370 feet and the majority 
of them about 250 feet. At about 100 feet salt water was 
usually struck, but the brine was weaker than that obtained 
at a greater depth. 

In many places the salt water has been obtained by inclosing 
a space 8 or 10 feet square by driving down piling of 2-inch 
boards, and then digging out the dirt from the interior, when 
the salt water would gradually fill the shafts. The dug wells 
were, of course, located on the spots where the salt water oozed 
from the ground. The brine from the dug wells is reported 
to be relatively weak. 



WATERS OF THE TERTIARY 301 

A story vouched for by a number of witnesses is to the ef- 
fect that during the boring of one of the wells on Salt Creek 
there was a great explosion or "blow-out" of gas, which tore 
up the casing and made a noise which was heard for miles. 
With the explosion came a great rush of gas which caught 
fire from a camp near by and striking back to the well set fire 
to the derrick, consuming It. 

All the wells on the Washington County side of the Tom- 
bigbee seem to be located on the strata of the Claiborne forma- 
tion (upper or lower), and to penetrate into the Hatchetigbee 
beds, except of course the shallow dug wells, which do not go 
deeper than 25 or 30 ieet. The hills bordering all the salt 
flats seen by the writer were of the St. Stephens limestone, and 
rocks of the nature of the radiolarian clay stones so character- 
istic of the lower Claiborne or Buhrstone were noticed in manv 
instances close to the well, with apparently hardly space enough 
for the upper Claiborne strata to come between them and the 
white limestone. About the Bucksnort Works, near Peevy's 
Landing, however, the upper Claiborne beds are well exhibit- 
ed along the road leading down to the river. 

Most of the salt wells of this county and of Clarke County, 
on the opposite side of the river, yield a small amount of na- 
tural gas with the brine, and many of the weaker brines are 
also strongly charged with sulphuretted hydrogen. These 
circumstances have led recently to the boring of a number of 
deep wells in this section in search of petroleum. Several of 
these borings were made along the reef of rock which forms 
the McGrew Shoals, above St. Stephens. It is stated that many 
years ago, when a blast was made in this reef to clear the shoals 
for navigation, oil came out of the rock upon the surface of the 
water in the river and was ignited and burned there for some 
time. This statement was made in a newspaper at the time 
of the occurrence. Several recent borings have been made on 
both sides of the river in this vicinity. 

ST. STEPHENS. 

Concerning the borings of the Washington County side, a 
few notes have been obtained from Mr. B. D. Turner and from 
Mr. James Keoughan, the contractor: 



302 DETAILS : COASTAL PLAIN DIVISION. 

St. Stephen's Oil Company's well, in Section 27, Township 
7, Range 1 W., in the northwest corner of the old Spanish 
grant. known as the John McGrew tract, about 1,600 feet 
from the oil landing on Tombigbee River, above St. Stephens ; 
bored in 1902; depth, 2006 feet; casing, 700 feet, 8-inch. No 
accurate log of this boring was kept and the following notes 
are from memory. At the depth of 250 feet, salt water and 
gas (Turner), below which was a very hard layer of "Buhr- 
stone" rock 5 feet thick. Below this to 1,250 feet, alternations 
of hard ledges and sands with salt water and inflammable gas. 
At 730 feet a heavy flow of fresh water in white sand 
(Keoughan). A heavy flow of salt water and gas was noted 
by Captain Keoughan between 750 and 800 feet. At 1,250 
feet, according to Mr. Turner, the fluid from the boring 
changed from lead color to black, probably because of a bed 
of lignitic matter. Below this to the bottom of the well were 
750 feet of dark-blue sand and blue shale. 

The St. Stephens limestone lies on the hills about this well, 
which is in one of the palmetto flats bordering a small stream 
emptying into the. river close by. The mouth of the well ap- 
pears thus to be in the Claiborne strata close below the base 
of the St. Stephens. The salt water at the depth of nearly 800 
feet would appear to be from strata below the Hatchetigbee 
which has generally been considered the main reservoir of the 
salt waters, and certainly is for many of them. The bottom 
of this boring is probably in the Cretaceous limestone. 



MOBILE COUNTY. 

Surface Features. 

The geologic formations which show at the surface in Mo- 
bile County are the Grand Gulf and Lafayette, with the later, 
comparatively recent lowland formations or bottom lands of 
the rivers and creeks. 

The St. Stephens limestone passes below the Grand Gulf for- 
mation in the upper part of Washington County and is not 
see at all in Mobile County. The existence, however, of ma- 
rine Miocene strata far below the surface in the latitude of 
the city of Mobile is proved by the shells brought up from 



WATERS OF THE TERTIARY 303 

the deep wells bored in several parts of the city, which will be 
referred to later. None of the borings as yet recorded has 
gone down into the St. Stephens limestone. 

The most prominent topographic feature of Mobile County 
in some respects is the Citronelle-Springhill ridge, the water- 
shed between Mobile and Dog rivers. This ridge, with con- 
stantly diminishing altitude, extends down to within 2 or 3 
miles of the Gulf. At Citronelle its altitude at the railroad 
station is 333 feet, while elevations on both side of the road 
are as much as 30 feet higher ; at Springhill, (> miles west of 
Mobile, it is 2 It) feet; and at St. Elmo station, on the Louis- 
ville and Nashville Railroad, it is 130 feet in a cut of 30 feet, 
making the land surface 160 feet above tide. 

The width of the ridge varies as the headwaters of the sev- 
eral branches of the two drainage systems approach or recede 
from the central line of the divide, being in some palces a 
mere "backbone," in others a plateau a mile or two in width. 
From this divide there is a gentle descent into the broad ''sec- 
ond bottoms" of Mobile River on one side and of Dog River 
on the other. 

Away from the level lands capped with the Lafayette loam 
and pebbles, the clayey sands of the Grand Gulf are everywhere 
the surface strata except in the near vicinity of the coast and 
streams. Wherever this is the case in Mobile, Washington, 
Baldwin, and Escambia counties, and probably elsewhere, the 
generally level surface is marked by numerous shallow depres- 
sions which are filled with water in wet seasons, becoming 
ponds or marshes, or, where not too wet, meadows or savan- 
nahs. 

Where the Lafayette is the surface formation an abundance 
of the best freestone water is obtained from open wells or 
from springs which break out along the hillsides at the con- 
tact of the Lafayette with the underlying Grand Gulf beds. 
Most of the streams flowing away from the Citronelle ridge 
have their headwaters in such springs or oozes from the La- 
fayette sands. Some of these springs are celebrated, such as 
that at the Jesuit college at Springhill ; others are less well 
known, but quite as fine. On account of the pure water and 
fresh air, Springhill is much visited by the citizens of Mobile, 
many of whom have their residences there. 



301 details: coastal plain division. 

Mineral Wateks. 



CITRON ELLE. 



In the territory of the Grand Gulf formation, i. e., in the 
lower-lying lands from which the Lafayette capping has been 
removed by erosion, the water conditions are rather unfavor- 
able, for while an abundant supply can usually be obtained by 
boring through the superficial layers into the underlying clays, 
yet it is often charged with mineral matter and objectionable 
to the taste. Frequently these waters break through the sur- 
face layers forming bold springs, often mineral springs. Of 
such character is the Cherokee or Wedgeworth Spring, 2 or 
3 miles east of Citronelle, but many feet below the level of the 
ridge. This is -a strong chalybeate and sulphur water, as is 
shown in the analysis by Mr, Hodges, given below : 

Analysis of water from Cherokee Spring, 3 miles east of Citronelle. 



Parts per million. 

Potassium (K) .9 

Sodium (Na) 4.0 

Magnesium (Mg) 1.1 

Calcium (Ca) : 3.0 

Iron (Pe) 12.6 

Alumina (ALO s ) -.8 

Chlorine (CI) 3.5 

Sulphuric acid (S0 4 ) 2.1 

Carhonic acid (HC0 3 ) 45.6 

Silica (Si0 2 ) 17.9 

91.5 _ 



SPRINGS NEAR THE COAST. 

In the flat lands near the coast there are many mineral 
springs and some of the wells in the same section, both shallow 
and artesian, yield similar water. 

Bromberg's springs. — Near Bayou Labatre, on the land of 
F. G. Bromberg, of Mobile, are several springs of clear, cool 
water, some of them almost on the banks of the bayou. The 
following analysis, by Mr. Hodges, is of the water from one 
of these springs: 



WATERS OF THE TERTIARY 305 

Analysis of water from Bromberg's spring No. l, near Bayou Labatrc. 



Parts per million 

Potassium (K) 1.7 

Sodium (Na) 3.7 

Magnesium (Mg) .9 

Calcium (Ca) .6 

Iron (Fe) 2.3 

Chlorine (CI) 12.7 

Sulphuric acid (S0 4 ) 1.4 

Silica (Si0 2 ) 6.4 

29.7 



It is rarely that an analysis shows so small proportion of dis- 
solved solids. From this point of view the water would be 
called remarkably pure, and its color and taste bear out this 
inference. 

Another of these spring waters has been analyzed by the 
National Brewers' Academy and Consulting Bureau of New 
York,* as follows : 

Analysis of water from Bromberg's spring No. 2. near Bayou Labatre. 



Parts per million. 

Sodium (Na) 5.10 

Potassium (K) 32 

Magnesium (Mg) 1.25 

Calcium (Ca) 1.15 

Chlorine (CD 9.27 

Sulphuric acid (SO t > 2.18 

Carbonic acid (HCO s ) 15.08 

Iron (Pe) 88 

Lithium (Li) 13 

Organic carbon .48 

Silica (Si0 2 ) 6.08 

41.92 



The analyses show these two waters to differ very material- 
ly. In the first the salts are chlorides only, with the exception 
of a small amount of sulphate of iron ; in the second the salts 
are chlorides, sulphates, and carbonates. In both, on the other 
hand, the salts of magnesium and iron and common salt pre- 
dominate. 

*Expressed by analyst in grains per gallon and hypothetical com- 
binations ; recomputed to ionic form and parts per million at U. 
S. Geological Survey. 

20 



306 DETAILS : COASTAL PLAIN DIVISION. 

Grand Bay. — Of somewhat similar character to the water 
from Bromberg's spring No. 2 is that from a shallow well in 
the northwest corner of the S. half N. E. quarter Section 6, 
Township 7, Range 3W., on land belonging to John W. Bright, 
of Grand Bay. This is a well bored with an auger, 24 feet 
deep, curbed with plank and admitting a bucket 6 inches in 
diameter; it yields 50 gallons, and after an interval of 12 hours 
the water is up to the original stand. On account of its taste 
and the fact that it stained vessels in which it stood, it was 
thought to have medicinal value. It is a strong chalybeate 
water, as the following analysis by Mr. Hodges shows : 

Analysis of water from John W. Bright' s well. Grand Bay. 



Parts per million. 

Potassium (K) 2.4 

Sodium (Na) 26.5 

Magnesium (Mg) .2 

Calcium (Ca) 4.1 

Iron and alumina (Fe 2 3 , A1 2 3 ) 24.4 

Chlorine (CI) 28,3 

Sulphuric acid (S0 4 ) 1.4 

Carbonic acid (HC0 3 ) 42.1 

Silica (Si0 2 ) 35.0 

164.4 



SPRINGS ABOUT MOBILE BAY. 

Along the Mobile terrace and in other low grounds about 
Mobile Bay a plentiful supply of water can commonly be ob- 
tained by driving tubes down to depths of 75 feet or more, 
but the character of the water varies with the locality. On 
the river front, according to Mr. N. K. Ludlow, extremely 
salty water was obtained at a depth of 40 feet, while at 75 feet 
in the same locality the water was free from salt and good for 
all uses. At the light-house and also immediately opposite the 
city of Mobile a pipe driven to the depth of 150 feet yielded 
only clear salt water. At the light-house the water rose in 
the tube to within 18 inches of the top: The strata passed 
through were, first, a river-mud deposit, then a hard blue clay, 
with sand below it; at 150 feet a hard rock was encountered 
and through which it was impossible to drive the tube. Mr. 
Ludlow is of the opinion, based on his personal experience, that 



WATERS OF THE TERTIARY 307 

it is impossible by any ordinary band or steam pump to ex- 
haust the water from a driven well properly put down in this 
section. 

These waters probably all come from the comparatively re- 
cent deposits overlying the Lafayette and Grand Gulf along 
the terraces of streams and the Gulf or Bay. 

Artesian Prospects. 

Experience of recent years has shown that artesian water 
can be had in most parts of the county where the elevation is 
not too great. These Later borings have demonstrated the 
fact, heretofore unknown, that a great thickness of marine 
Tertiary deposits, of Miocene and later age, underlies the lower 
half and in all probability the whole of the county. The bor- 
ings also demonstrate the fact, which can easily be verified by 
any one who will drive a few miles around the city of Mobile, 
that the deposits which have for many years been recognized 
by the geologists of the Gulf coast as Grand Gulf overlie all 
these later Tertiary beds, even down to the waters of the Gulf 
of Mexico. In Baldwin County this evidence is even more 
convincingly presented in the easily recognized Grand Gulf 
exposures in high bluffs overlooking the waters of Mobile 
and Perdido bays. 

In many of these waters the proportion of salt is high, but 
in others it is not so great as to unfit them for ordinary uses. 

MOBILE AND VICINITY. 

Well at Mobile Brewery, Corner of Water and Adams streets, 500 yards 
from river front; depth, 800 feet; bored by Elder Hydraulic Boring Com- 
pany in December, 1894. This was one of the first of the artesian wells 
in this county. After passing through a deposit of the "second bottom'' 
or terrace formation, including probably the Lafayette, the boring goes 
through beds which can be identified only with the Grand Gulf, into 
shell-bearing strata which are shown by well-preserved fossils to be of 
late Tertiary age. Record furnished by Dr. Charles Mohr. 



308 DETAILS : COASTAL PLAIN DIVISION. 

Record of Mobile Brewery well. 



Depth, (feet) 
Coarse, sharp-edged sand, with siliceous pebbles and fragments of 

oyster shells yo 

Fine sand 100 

Coarse gravel of siliceous pebbles and coarse sand, with lignitized 

coniferous wood 130 

Muddy sand; water highly charged with bluish-green argillaceous 

matter 300 

As above, more compact, sandy particles somewhat finer and plastic 450 

Of the same muddy nature, compactness increasing 490 

Arenaceous sediment in the blue still finer, more plastic; dL.cult 

boring 580 

Sediment still more plastic, very fine, soft and velvety 62b 

Material remains unchanged 660 

Stratum of indurated clay, with some coarse sand, abounding in 

small bivalves; small flow of water 700 



After penetrating the clay about 30 feet a heavy stream of water was 
struck, with a discharge estimated at not less than 300 gallons per min- 
ute, under heavy pressure, bringing up pebbles of large size, indurated 
clay nodules. The material resembles the shingle of a beach. Also an 
abundance of coarse black sand (with magnetic iron ore). Two days 
later the flow of water had increased to 500 gallons per minute, and was 
about clear of sand. 



Well of the Mobile Electric Lighting Company, bore in 1906. Depth, 
650 feet; diameter, 8 inches; flows a large volume of water of brownish 
color and slightly brackish taste, accompanied by a little inflammable gas. 

Well at the oil mill, 3 miles north of Mobile; depth, about 800 feet: 
record similar to that of the Brewery well, so far as can be ascertained. 
The water from this well is salty and accompanied by a considerable 
amount of marsh gas. The following analysis of the water was mans 
by James Boyce, chief chemist of the American Cotton Oil Company.* 

Analysis of water from Cotton Oil Mill Company's well, 3 miles north 

of Mobile. m 



Parts per million. 

Sodium (Na) 1135.52 

Potassium (K) 15.74 

Magnesium (Mg) 7.40 

Calcium (Ca) 15.10 

Chlorine (CI) 1440.44 

Carbonic acid (CO a ) 281.30 

Silica (Si0 2 ) 19-20 

Organic matter • 178.30 

3,093.00 



*Expressed by analyst in grains per gallon and hypothetical com- 
binations: recomputed in ionic form and parts per million at U. S. 
Geological Survey. 



WATERS OF THE TERTIARY 309 

Wells of Blacksher Lumber Company, at Magazine, three miles north of 
Mobile at the mouth of Chickasabogue creek. Bored by J. A. Joullian 
in 1906. 

No. 1. Depth, 250 feet; diameter, S-inches; flow 75 gallons per minute. 
The water being intended for boiler use was analyzed and found to 
contain considerable quantities of the sulphates of sodium and potas- 
sium and practically no iron. It is highly prized both for drinking and 
for use in the boilers. No. 2. Depth, 420 feet; diameter, 3-inclies. First 
water at 250 feet; second at 390 feet, from which depth the water is 
taken. 

Plow and quality of the water similar to that of No. 1, except that the 
water has a slightly brackish taste, and is accompanied by a small 
amount of inflammable gas. Record; white sand and red clay, 0-100 
feet; blue clay, 100-250 feet, at which depth the first water was obtained 
in sand. Below the depth of 250 feet the record is not given, but at 420 
feet a bed of black or dark clay was entered from which some frag- 
ments of shells broken by the drill, were obtained. 

Mobile Oil Company's wells, at the Bascomb race track, a 
few miles from the court-house near Mobile ; bored by J. A. 
Joullian in 1902; two wells close together; records practically 
identical. 

Record of Mobile Oil Company's well No. 1, near Mobile. 



Material. Thickness. Depth. 

Feet. Feet. 

Upper soil 15 15 

Blue clay 10 25 

Lignite 2 27 

Blue clay and sand 75 102 

Coarse white sand 15 117 

Gravel 35 152 

Stiff blue clay 22 174 

Blue sand 6 180 

Blue shale and fragments of shells 22 202 

Blue clay 52 254 

Sand 5 259 

Blue clay 15 :', 1 

Coarse white sand 46 320 

Blue shale and shells 20 340 

Blue shale 35 375 

Sandstone 3 378 

Gravel 1 379 

Gumbo 15 394 

Blue sand 10 404 

Blue shale 5 409 

Sandy blue clay 45 454 

Blue clay 23 477 

Sand 15 492 

Blue shale 29 521 

Sand 10 531 

Blue shale 40 571 

Gravel 5 576 

Blue shale 50 626 

Blue shale with shells 2 628 

Blue clay 20 648 

Sand 22 670 

Blue shale and lignite 2 672 

Blue shale and rotten shells 20 692 

Sand, shelly 20 712 

Shale 19 731 



310 details: coastal plain division. 



Gumbo 20 751 

Shale, shells 20 771 

Shale and small shells 9 780 

Blue clay 30 810 

White sand 5 815 

Gumbo 25 840 

Sand, salt water, and gas 59 899 

Gravel 47 946 

Gray clay 21 967 

Blue clay 17 984 

Shale and shells 23 1,007 

Sand 23 1,030 

Blue clay 29 1,059 

Blue shale 11 1,070 

Blue clay 22 1,092 

Conglomerate, pebbles 2 1,094 

Hard blue shale 16 1,110 

Sand rock 2 1,112 

Gumbo 36 1,148 

Sand rock 5 1,153 

Gumbo 3 1,156 

Sand rock 8 1,164 

Gumbo 5 1,169 

Sand rock and some gas 4 1,173 

Blue clay and lignite 23 1,196 

Hard rock 4 1,200 

Gumbo 12 1,212 

Rock 2 1,214 

Gumbo and lignite 10 1,224 

Rock 7 1.231 

Fine sand 5 1,236 

Rock 2 1,238 

Blue clay and shells : 8 1,246 

Gumbo 12 1,258 

Shale 25 1,283 

Rock ...' 2 1,285 

Gumbo 23 1,308 

Shale 45 1,353 

Gumbo 85 1,438 

Limestone, blue 2 1,440 

Shale 1 1,441 

Limestone 2 1,443 

Shale 4 1,447 

Shale 2 1,449 

Limestone 1 1,450 

Shale 2 1,452 

Lime rock 7 1,459 

Sand and shells; gas and saltwater .. 60 1,519 

Limestone 7 1,529 



Shells were brought up from various' depths in this well. At' 
about 700 feet the shells indicate the Pliocene; between 1500 
and 1550 feet were shells characteristic of the Oak Grove 
CFla.) horizon, which is Miocene. 

Well No. 2 (Plate XXVIII) went deeper, pentrating into 
the Chattahoochee limestone, though not reaching the Vicks- 
burg (St. Stephens.) In this well also, at the depth of 1,250 
feet, the shells encountered were those characteristic of the 
Chipola beds of Florida. Thus there is here a section of the 
Pliocene and the whole of the Miocene of the Gulf coast. These 
beds are very sparingly exposed at the surface in Alabama; the 
only locality thus far noted being in Escambia County; but 



WATERS OF THE TERTIARY 311 

they are well shown on the Chattahoochee River in Florida, 
and on the Chickasawhay in Mississippi, where, however, they 
are only the uppermost of the series which has been identified 
as Pliocene. 

Great quantities of salt water and inflammable gas come up 
from both these wells. The following notes on well No. 1 are 
furnished by Mr. Joullian, who superintended the work. 

The well has a flow of 2,500 barrels (of 42 gallons) in twen- 
ty-fonr hours. The water is a 3 'per cent, salt solution, with 
a temperature of 86*. The well also yields about 200,000 cu- 
bic feet of gas in twenty-four hours. It was the intention to 
pipe this gas to the city, but it has 1 not been done. As the water 
spouts up 7 or 8 feet above the end of the 4-inch pipe which 
forms the casing it is a foam of gas and water which can 
be ignited, when it burns until accidentally splashed out by the 
water falling back. 

ALABAMA PORT. 

At Alabama Port, near the southeast end of the mainland, 
below Mobile, a well has been bored by the company owning 
the property. From this well also shells have been brought 
up which identify the formations as in the other wells above 
noticed. The water from this well has been analyzed by Mr. 
Hodges, with the result shown below : 

Analysis of water from well at Alabama Port. 



Parts per million. 

Potassium (K) trace 

Sodium (Na) 120.2 

Magnesium (Mg) trace 

Calcium (Ca) 2.6 

Iron and alumina (Fe 2 3 , A1 2 3 ) 1.1 

Chlorine (CI) 113.7 

Sulphuric acid (S0 4 > 1.0 

Carbonic acid (HCO,) 129.1 

Silica (Si0 2 ) 33.5 

401.2 



No accurate record was kept of this boring, but the follow- 
ing notes are furnished by Mr. L. M. Tisdale : Flowing water, 
7 gallons per minute, was struck at 80 feet, the small flow be- 
ing due to a defective strainer. The present well is cut off 



3J2 details: coast \l plain division. 

at 377 feet, below which to the bottom (900 feet) hard ledges 
were encountered at intervals in the generally loose and un- 
consolidated materials. 

Another well is now (1905) in progress in the name locality. 

FORT GAINES. 

At Fort Gaines, at the east end of Dauphin Island, across 
the channel from Fort Morgan, a well has recently been bored 
by the United States Government. It was completed November 
12, 1903; diameter, 6 inches; depth, 919 feet. 

Record of Government well, Fort Gaines. 



Material Thickness. Depth. 

Feet. Feet. 

White sand 10 10 

Black sand 60 70 

Blue sand 6 76 

White sand 7 95 171 

Blue clay 20 191 

White sand 41 282 

Blue sand, very fine 45 277 

Blue clay 35 312 

Blue sand : 30 342 

Blue clay 10 352 

Limestone (2 feet) 2 354 

Gray sand; salt water 55 409 

Sandstone, very hard 5 414 

Gravel 5 419 

Gumbo clay 30 449 

Gray sand 110 559 

Blue clay 60 619 

Gray sand 50 669 

Gravel 10 679 

Blue clay 145 824 

Water-bearing- sand (strainer landed in 

this) 95 919 



The water from this well has been analyzed by Mr. Hodges, 
with the result given below : 

Analysis of water from Government loell. Fort Gaines. 



Parts per million. 

Potassium (K) 4.1 

Sodium (Na) 126.7 

Magnesium (Mg) 1.4 

Calcium (Ca) 6.1 

Iron and alumina (Fe 2 3 , A1 2 3 ) ' 1.6 

Chlorine (CI) 192.9 

Sulphuric acid (SCO 2.0 

Carbonic acid (HCO a ) 29.1 

Silica (SiOo) 53.9 

416. S 



GEOLOGICAL SURVEY OF ALABAMA. UNDERGROUND WATER RESOURCES. PLATE XXIX. 





Artesian well, Oyster Canning Establishment, near Bayou La Batre, 

Mobile County'. 



WATERS OF THE TERTIARY 313 

WELLS ON POBTERSVILLE BA"S SHORE. 

The following six records are available of wells bored along 
the Bay shore from the mouth of Bayou Labatre to a point a 
little east of the mouth of Bayou Coden. Those nearest Bayou 
Labatre were bored several years ago, the others in 1906. 

Oyster Canning Establishment well, at mouth of Bayou Labatre. Only 
meagre records can be obtained of this well which was bored a number 
of years ago. It is 580 feet deep, passing through sands and clays. The 
first water was reached at 500 feet, but the yield was small and the water 
rose only to the top of the tube. The boring was then continued for 40 
feet, when the drill dropped suddenly 20 feet as if in a cave. Water was 
struck again at the depth of 5S0 feet, rising 15 feet above the surface, 
filling an elevated tank dire*ctly from the pipe. From the tank it is con- 
ducted by wooden troughs supported on trestles to the factory, on-i- 
fourth mile or more distant. Plate XXIX shows this arrangement. 

The water from this well is quite different in composition from that 
of the Fort Gaines well, but similar to, though less salty than that of 
the Alabama Port well, as may be seen from the accompanying anal- 
ysis by Mr. Hodges: 

Analysis of water from Bayou Labatre Cannery iccll. 



Parts per million. 

Potassium (K) 3.7 

Sodium (Na) 54.5 

Magnesium (Mg) 1.1 

Calcium (Ca) 3.5 

Iron and alumina (FeoOs. AU0 3 ) 1.8 

Chlorine (CD 42.5 

Sulphuric acid (S0 4 ) 4.0 

Carbonic acid (HC0 3 ) 87.9 

Silica (SiO a ) 48.7 

247.7 



Another well of which no records have been obtained has been bored 
near the railroad track a few rods north of the Oyster Cannery well above 
described. 

Barret's well near Sans Souci Beach. Depth, 518 feet; diameter, 2 
inches; flow, 50 gallons per minute. The water unlike that of the Mobile 
wells is clear and without color; contains sulphate of sodium and a little 
iron and sulphuretted hydrogen. 

The Graham well at the mouth of Bayou Coden. Depth, 520 feet; diam- 
eter, 3 inches; flow, 100 gallons per minute, a full strong stream, under 
considerable pressure. The water has a slightly stronger taste of sul- 
phate of sodium than the preceding. 

Well at Coden station where the railroad crosses Bayou Coden. Depth, 
about 520 feet, good flow, record similar to that of the other wells along 
the beach. 

The Ralston well on the beach a short distance east of the Mouth of 
Bayou Coden and the Graham well. Depth, 520 feet; diameter, 3 inches 



314 DKTAILS: COASTAL PLAIN DIVISION. 

flow 60 gallons per minute; water of the same quality as that of the 
Barret well. 

Record of the Portersville Bay wells ahove described; Soil and mottled 
clay, 0-15 feet; Blue clay, 15-48 feet; sands yielding abundance of water, 
not overflowing, 48-68; Blue clays alternating at intervals with sands, 
all devoid of shells or other organic remains so far as could be seen, 
68-520 feet. 

CITRONELLE. 

On the high plateau dividing the waters ot the Alabama 
from those of Dog River, near Citronelle borings were made in 
1902 in search of oil, under the auspices of the Mobile Oil 
Company. Two wells were sunk not far apart. The second 
well went to the depth of 1,960 feet or more. A few notes in 
regard to this well have been obtained from Mr. Knott, who 
did the drilling. From the surface down to 900 feet the ma- 
terial appeared to be sand and shale (clay ?) ; at 900 feet a 
blue marl was encountered, and at that depth Mr. Knott found 
a little showing of oil; from 900 to 1,960 feet there were al- 
ternations of rock and shale and streaks of dry sand ; between 
500 and 600 feet there was plenty of water, but it was not 
tested as to whether or not it would overflow. No water was 
found below 650 feet. 

As has been stated above, the surface materials of the Cit- 
ronelle plateau are the red loam, sand, and pebbles of the La- 
fayette, beneath which is an undetermined thickness of sands 
and clays of the Grand Gulf formation, at least 300 feet, to 
judge from, the fact that the same formation is at the surface 
on the river banks 300 feet lower, in the same latitude. 



BALDWIN COUNTY. 

Surface Features. 

So far as observation has yet gone, nothing older than the 
Grand Gulf shows at the surface in Baldwin County, which 
extends 72 miles north and south. Over the Grand Gulf lies 
the mantle of Lafayette loams, sands, and pebbles on most of 
the higher, least-eroded divides ; not indeed in a continuous 
sheet, but in patches which are remnants of such a sheet. 
In topographic character the county varies from hilly and dis- 
sected in the northern half to high-level plateaus in the south- 



WATERS OF THE TERTIARY 315 

ern half. These high flat lands extend to the shores of Mo- 
bile and Perdido hays, ( Plates XVIII, XIX, and XX). The 
elevation of the land between Mobile Bay and Perdido River 
south of the main line of the Louisville and Xashville Railroad 
is on an average not less than 200 feet. 

The flat lands above mentioned are characterized by the oc- 
currence at frequent intervals of shallow depressions, which, 
according to the season, are shallow ponds, marshes, or sa- 
vannahs. (Plate XXII). The larger and more permanently 
wet depressions are the well-known "gum ponds," so called 
from the fringe of black gum trees with they are bordered. 
(Plate XXI). The gently undulating surface thus produced, 
with its timber of long : leaf pine, its lack of shrubbery under- 
growth, and its carpet of grass, resembles a well-kept park. 

Shallow Waters. 

Water is easily obtained in nearly all parts of the county — 
from springs where the inequalities of the surface are suffi- 
cient to expose the Grand Gulf beds below the Lafayette, and 
elsewhere from open wells which vary in depth from a few 
feet to 90 feet. In the northern half of the county the condi- 
tions are like those so often described in the other counties. In 
the southern half the flatness of the country causes a relative 
scarcity of springs. Below the Lafayette the stratified sands 
and clays of the Grand Gulf afford storage reservoirs, and 
bottoms for the open wells. At Daphne, opposite Mobile, the 
wells are 40 to 45 feet deep, passing first through the Lafay- 
ette loams, then into Grand Gulf sands to water, which is 
always just above streaks of pipe clay. At Randall's store, 
on the hill above Daphne, the wells are 100 feet deep, the 
extra depth being in the sands and loams above the stratified 
clay. On the high flats 3 or 4 miles from Daphne the wells 
again are shallower, 40 feet or more, passing through the La- 
fayette and the sandier beds of the Grand Gulf to a bottom of 
clay. At Montrose, south of Daphne, the wells are 90 feet deep 
only 200 to 300 yards back of the high bluff on which the set- 
tlement stands. This bluff is a part of the high land of the 
county, extending down to the bay without any intervening 
low grounds. It is well shown in Plate XVIII. 



316 details: coastal plain division. 

Mineral Waters. 

The mineral waters in Baldwin County are in the main 
salty. They are to be had from shallow and driven wells sunk 
on the sand spits and low islands. All the bored wells on 
Blakely Island are reported by Mr. J. D. Webb as yielding 
salty water. Shallow wells on the spit between the lagoon and 
the Gulf yield salt water from which salt was manufactured 
during the war. It is said to be more salty than the water of 
the Gulf. Some of these salt wells are in the N. E. quarter 
Section 12, Township 9 ,S., Range 3 E., on the eastern side of 
Bay St. John. Others are in the N. W. quarter Section 7, 
Township 9 S., Range 4 E. It is worthy of remark that simi- 
lar shallow wells on the mainland and quite as near to the 
salt water of the lagoons and bays frequently yield pure water, 
some of it exceptionally so. This may be seen in the analyses 
of the water from the Bromberg springs, and from the Bayou 
Labatre Cannery well, in Mobile County. Good drinking wa- 
ter is also to be had from shallow wells on the landward mar- 
gin of Perdido Bay in Baldwin County. 

Artesian Prospects. 

Except in a few deep wells recently bored the artesian con- 
ditions of Baldwin County depend on the strata of the Grand 
Gulf formation alone. Near Soldier creek Post-office, in Sec- 
tion 16, Township 8 S., Range 6 E., on Perdido Bay, in Mr. 
Randolph's driven well, 45 feet deep, the water rises very 
nearly to the surface. At Millview, on the Florida side of the 
bay, in a well 55 feet deep, the water rises 5 or 6 feet above 
the surface. Up Wolf Bay, near Swift Post-office, overflowing 
water is obtained at a depth of 110 feet. Near Perdido River 
at Lane's Ferry two flowing wells were noted and one at 
Gateswood, not far from Seminole. Of these no particulars 
were obtained. On the Florida side of the river such wells 
are more numerous than on the Alabama side. 

In the matter of deep wells there is comparatively little to 
record. In the southern part of the county, in the center of 
Section 22, Township 8 S., Range 4 E., Major Fitzhugh has 
recently bored for oil to a depth of of more than 1500 feet; 
record not obtained. It is of interest to< note that Miocene 
shells were encountered in this well, as in the Mobile wells, 
at depths of 730 feet and lower. 



WATERS OF 1IIIC TERTIARY 317 

SUPPLEMENTARY NOTES. 

ADDITIONS. 

Several analyses overlooked at the time or available since 
the printing- of that part of the Report to which they belong, 
are here added. 

Appalachian Valleys. 

Cahaba River Water. — The following analysis by Mr. Hod- 
ges, of water from Cahaba River at DeShazo's Mill, below 
Leeds in Jefferson county, is given as showing the average 
character of the water supply of the City of Birmingham. 
This belongs to the bicarbonated alkaline calcic class' of waters 
which includes the majority of the potable waters investigat- 
ed by us. 

Analysis of water from Cahaba River, below Leeds, Jefferson County. 



Parts ner million. 

Potassium (K) 3.6 

Sodium (Na) 3.8 

Magnesium (Mg) 8.0 

Calcium (Ca) 40.7 

Iron and alumina (Feo0 3 , AL0 3 ) 3.2 

Chlorine (CI) 3.5 

Sulphuric acid (S0 4 ) 1.7 

Carbonic acid (HC0 3 ) 162.2 

Silica (Si0 2 ) 46.1 

272.8 



Valley op the Tennessee. 

Sanaqtta Mineral Water, Huntsville, Madison County — In 
the vicinity of Huntsville, several rather shallow bored wells 
have recently been sunk into the limestones of the Subcar- 
boniferous formation. One of these is reported 3 miles' north- 
west of Huntsville of which no record is available. Another 
about 4 miles southwest of the city, was bored in 1905 by Judge 
S. Morgan Stewart. Depth 160 feet ; 40 feet through the sur- 
face soil and 120 feet into the limestone. The water stands al 
-no feet and is brought to the surface by a pump, the tubes 



318 details: coastal plain division. 

of which are very quickly corroded. Because of its very decided 
mineral qualities this water has been put on the market as the 
Sanaqua Mineral Water. Its composition is shown by the fol- 
lowing analysis made by Dr. B. B. Ross, State Chemist, the 
analysis being originally expressed in grains per gallon and 
hypothetical combinations', but lecomputed in ionic form and 
parts per million by Mr. R. S. Hodges. 

Analysis of Sanaqua Mineral Water, HuntsviUe, Madison County. 

Parts per million. 

Potassium (K) 22.5 

Sodium (Na) 2634.7 

Magnesium (Mg) 187.4 

Calcium (Ca) 410.7 

Ferrous oxide (PeO) 8.4 

Alumina (A1 2 3 ) 10.8 

Chlorine (CI) 1365.3 

Sulphuric acid (S0 4 ) 5393.0 

Carbonic acid (HC0 3 ) trace 

Sulphuretted hydrogen (H 2 S) 69.0 

Silica (Si0 2 ) 16.3 

10118.1 



As the analysis shows this is a strong saline water of the 
sulphated sulphuretted class, containing also a high percentage 
of sodium chloride and of salts' of iron. In these characters it 
resembles the waters of the Flatwoods of Sumter county as 
exhibited in the analyses of the waters of the Altaian, Mills, 
and Histitower wells. 



Coastal Plain Division; Cretacious. 



HALE COUNTY. 

Spring of T. G. Moore ; two miles from Greensboro in the S. 
W. quarter of the S. W. quarter of Section 7, Township 20, 
Range 5 E. This may be taken as a fairly representative 
spring of the kind mentioned on page 158 as coming from the 
Lafayette formation. The water from this spring has been 
analyzed by Mr. Hodges with the following results : 



WATERS OF THE CRETACEOUS. 319 

Analysis of uater from T. G. Moore's Spring, near Greensboro, Hale 

County. 



Parts per million. 

Potassium (K) .6 

Sodium (Na) 4.3 

Magnesium (Mg) .6 

Calcium (Ca) 1.2 

Iron (Fe) .3 

Alumina (Alo0 3 ) 2.3 

Chlorine (CI) 2.9 

Sulphuric acid (SO.,) .fi 

Carbonic acid (HCO a ) 13.8 

Silica (SiOo) 11.4 

38.0 



It belongs to the class of alkaline bicarbonated waters which 
includes many potable waters as well as waters' of reputed 
medicinal virtue. 

Artesian zvell at Lock 5, now Lock 8, Black Warrior River. 
— On page 161 reference is made to two wells at this Lock, 
between Stewarts and Akron. 

The water from well No. 1 has been analyzed by Mr. Hod- 
ges with the results given below. 

Analysis of water from well Xo. 1. Lock 8. Black Warrior River. 



Parts per million. 

Potassium (K) 8.3 

Sodium (Na) 105". 4 

Magnesium (Mg) 15.2 

Calcium (Ca) 87.2 

Iron (Fe) 2.8 

Chlorine (CI) 1330.1 

Sulphuric acid (SO4) trace 

Carbonic acid (HCO s ) 805.1 

Silica (Si0 2 ) 15.8 

33S1.9 



This is a strong alkaline saline muriated water with rel- 
atively high percentage of iron. The almost entire absence of 
sulphates is to be remarked. 

J Veil at Evans Station. — The water from one of the earlier 
artesian wells at Evans station in Hale county has been analyzed 
by Mr. Hodges ; probably one of the E. S. Evans wells men- 
tioned on page 162. It is a good type of the alkaline saline 
sulphated class and as such is' here given, although more- 



320 details: coastal plain division. 

heavily charged with dissolved salts than the majority of the 
waters of this class, excepting- the sulphur waters. 

Analysis of water from well at Evans Station, Hale county. 



Parts per million. 

Potassium (K) 3.0 

Sodium (Na) 106.3 

Magnesium (Mg) 33.2 

Calcium (Ca) 84.2 

Iron and alumina (Fe 2 3 , A1 2 3 ) 1.9 

Chlorine (CI) 21.0 

Sulphuric acid (S0 4 ) 274.0 

Carbonic acid (HCO s ) 323.4 

Silica (Si0 2 ) 44.6 

891.6 



Coastal Plain Divison ; Tertiary. 



SUMTER COUNTY. 

Well of Dr. J. A. Beavers, one mile east of Cuba. — Drilled 
by Dr. J. A. Beavers in May 1905 in his yard to supply water 
for domestic use. Previous to this time malarial fevers had 
been prevalent in his family but since the well was sunk no 
case of sickness has occurred and Dr. Beavers • ascribes this 
to the use of the water, which is raised by means of a hand 
pump. This pipe is 1 1-4 inch in diameter. 

The analysis by Mr. Hodges shows this water to belong to 
the class of alkaline saline water with predominant sulphates 
but with a good percentage of chlorides, and relatively high 
content of iron. Waters of this class even when only slightly 
charged with these mineral matters are often considered to 
have medicinal value, as' for instance the waters of the Healing 
Springs in Washington county, Butler Springs in Butler, 
Mentone Springs in DeKalb, Hawkin's well supplying the 
Leeds Mineral water in Jefferson county, mentioned in this 
report. 



WATERS OF THE TERTIARY 321 

Analysis of water from Dr. -/. A. Hearers' well, Sumter county. 



Parts per million. 

Potassium (K) .6 

Sodium (Na) 4.7 

Magnesium (Mg) 1.9 

Calcium (Ca) 3.6 

Iron and alumina (Fe 2 3 , A1 2 3 ) 1.8 

Chlorine (CI) 6.6 

Sulphuric acid (S0 4 ) 8.4 

Carbonic acid (HC0 3 ) 14.1 

Silica (Si0 2 ) 9.5 

51.2 



CORRECTIONS. 

Several errors have escaped the proof reader, as is inevitable. 
The following are perhaps of enough importance to be pointed 
out and corrected : 

On page 79 the summation of the analysis of the Cold Spring 
water should be 301.7, instead of 301.9. 

On page 80 the summation of analysis of water from Harrell's well 

should be 29 8.7, instead of 298.2. 

The analyses on page 89 of the waters from Cook springs, No. 1 
"Sulphur spring" and No. 3, "Chalybeate" are here reprinted as 
they should be, as the best way to make the corrections. 

Analyses of water from Cook Springs. 



Parts per million. 

No. 1. No. 2. 

Sodium (Na) 30.2 11.0 

Potassium (K) 2.6 3.7 

Magnesium (Mg) 4.1 2.6 

Calcium (Ca) 22.6 11.7 

Iron & alumina (Fe 2 3 . A1 2 3 ) 2.8 10.8 

Chlorine (CI) 5.3 3.5 

Sulphuric acid (S0 4 ) 5.3 2.1 

Bicartaonic acid (HC0 3 ) 157.1 74.1 

Sulphuretted Hydrogen (H 2 S) .4 

Silica (Si0 2 ) 43.8 44.8 

274.2 164.3 



Corresponding changes should be made in the figures in the de- 
scriptive paragraph preceding the analyses. 

On page 99. The summation cf Analysis No. 1 should be 949.34 
instead of 947.80. 

On page 133 in the heading of the analysis — C. B. Mill's should 
be C. P. Mills'. 
21 



322 DETAILS : COASTAL PLAIN DIVISION. 

On page 142 the summation of Dr. Webb's analysis should be 
5345.36 instead of 5335.36. 

On page 143 the figures showing the proportion of Sodium in the 
water of Allison well should be 2999.0 instead of 540.2 — and the 
analysis correctly stated should be 

Analysis of water from Allison Lumber Company's well, near 
Bellamy. 



Parts per million. 

Potassium (K) 13.2 

Sodium (Na) 2999.0 

Magnesium (Mg) 43.1 

Calcium (Ca) 139.6 

Iron & Alumina (Fe 2 3 , A1 2 3 ) 5.2 

Chlorine (CI) 4538.0 

Sulphuric Acid (S0 4 ) .3 

Carbonic Acid (HCO s ) 784.5 

Silica (Si0 2 ) 50.8 

8573.7 



On page 160 the figure for Silica in the analysis should be 19.9 
instead of 19.2. 

On page 162 the summation of the first analysis of the Akron 
water should be 129.7 instead of 141.4, and that of the second, 
115.4 instead of 115.1. 

On page 258 — the summation of the analysis should be 209.68 
instead of 205.25. 

On page 276 the summation of analysis No. 3 should be 304.1 in- 
stead of 303.1. 



CHAPTER IV. 

THE CHEMISTRY AXD CLASSIFICATION OF 
ALABAMA WATERS. 

CHEMISTRY. 

We have seen that all underground waters have their source 
in the rainfall. Before reaching- the earth the rainwater is 
practically free from solid mineral matter, but is more or less 
charged with oxygen and carbon dioxide, which give to it 
some solvent power. At the surface its solvent powers are 
still further increased by the solution of certain compounds 
resulting from the decomposition of organic matter, and local- 
ly, from the oxidation of metallic sulphides (chiefly iron pv- 
rites). Aided by these it speedily becomes charged with min- 
eral matter in its downward percolation through permeable 
strata. 

All natural waters are therefore mineral waters, though this 
term has now come to include only those natural waters to 
which their mineral contents impart a decided taste or a decided 
medicinal quality. 

Let us first follow the course of the meteoric water, charged 
as it is with oxygen carbon dioxide, and organic matter, in its 
downward progress' through the strata. The sedimentary rocks 
which furnish to the infiltrating waters their mineral contents 
may for convenience be placed in two groups, namely : ( I ) 
those composed of the products of the decomposition more or 
less complete, of the crystalline rocks, and (2) those consisting 
essentially of limestone and dolomite. 

The materials of the first group are, the insoluble residual 
matters, (mainly quartz sand and clay, usually ferruginous), 
resulting from complete decomposition ; the undecomposed but 
still decomposable fragments of the constituent (especially felds- 
pathic) minerals of these rocks ; and the soluble products (main- 
ly alkaline carbonates and silicates) of this decomposition, per- 
meating and saturating the two preceding. 

These soluble products' and the gradual decomposition of the 
feldspathic fragments by the caibonated waters furnish a con- 



324 Chemistry and Classification of Alabama Waters. 

tinuous supply of the alkalies to the water. The carbonate 
of potassium, as is well kilown, in contact with clayey sediments, 
very quickly passes into insoluble compounds ; the carbonates 
of calcium and magnesium in this class of sediments although 
soluble, are present in very small quantities ; while the sand and 
clays are almost entirely insoluble. The carbonated water which 
has passed through sediments of this nature would therefore, 
contain notable quantities of sodium with smaller amounts of 
calcium and magnesium. 

In its circulation through the strata the carbonated meteoric 
water comes also in contact with the second class of sediments 
composed of limestones and dolomites, from which it takes 
up notable amounts of calcium and magnesium in the form of 
bicarbonates or as simple carbonates ; and such water would 
therefore be characterized by a predominance of calcium and 
magnesium ions, although waters' coming from limestones al- 
ways contain more or less sodium. 

In their underground circulation an intermingling of waters 
of these two varieties would naturally give rise to those inter- 
mediate classes containing carbonates both of alkalies (K and 
Na), and of alkaline earths' (Ci and Mg.) 

We have also seen that the great majority of our stratified 
rocks are marine sediments, and therefore must necessarily have 
the pore spaces which constitute no> inconsiderable portion of 
their volume, filled with the waters of the ancient seas in which 
the sediments' were deposited. This will be the case especially 
where these rocks lie below the level of the sea and have nor 
been uplifted or broken so as to allow their bitter waters to 
be replaced by fresh infiltrating waters. It may be remarked 
here also, that clayey and calcareous sediments preserve their 
saline solutions far better than do the porous' sandstones, as 
may be seen by comparison of the analyses of the water de- 
rived from strata of various kinds.* And furthermore, as at 
present, so in the past, there have been interior basins without 
outlet, and portions of the sea isolated from the main body in 
which bv complete evaporation, gypsum, salt, and the more sol- 
uble salts of the mother liquor have become incorporated in 
the sediments in solid form. Circulating waters after taking 
in solution these neutral salts from the above mentioned marine 
sediments, embrace on the one hand the brines, characterized 



*T. S. Hunt, Chemical and Geological Essays, page 104. 



Chemistry, 325 

by the preponderance of chlorides and the practical absence oi 
Sulphates, and on the other hand, the sulphated waters char- 
acterized by the predominance of sulphates and the relatively 
small amount of chlorides. Sulphated saline waters of this 
origin are, however, in our experience, rare. The more proline 
source of the sulphated waters is the action of the sulphuric 
acid and sulphates of iron and aluminum, generated by the oxi- 
dation of pyrites, upon salt-bearing calcareous and magnesian 
sediments'. Beds of carbonaceous clay with gypsum and iron 
pyrites are especially favorable to the production of such water 
as is shown by its abundance in the "Flatwoods" belt of the 
Tertiary. Often waters of this later class contain free sulphu- 
ric acid, there being all gradations between strongly acid waters 
nad those in which the free acid has been neutralized by the al- 
kaline and earthy constituents of the enclosing sediments. Those 
waters produced through the agency of the oxidation products 
of pyrites must necessarily be of superficial and local character, 
and, so far as we have examined them, come from springs and 
shallow wells, varying in composition with the saturation oi 
the acids and in concentration with the variations in rainfall. 

It goes almost without saying that a water deriving its min- 
eral constituents from any one of the above mentioned sources 
alone will rarely be met with, for in the underground circula- 
tion there must inevitably be a more or less thorough mingling 
of the waters enriched from all the sources referred to. 

The agency of decaying organic matter, such as is found in 
the black shales' of the Paleozoic formations, in the mineraliza- 
tion of water is shown in those varieties popularity designated 
as "chalybeate" and "sulphur" water. Small proportions of 
iron ore are present in almost every variety of water, but it 
is only to those in which a notable amount (8 parts per mil- 
lion* ) of iron is present and which therefore have characteris- 



*In the ease of waters containing only a small amount of mineral 
matters, iron in much smaller proportion, than 8 parts per million 
may impart a chalybeate character to it. The analyses given in this 
report seem to show that when the proportion of iron to the total 
amount of dissolved solids in the water is as high as 1 to 7">, the 
water is chalybeate. 

Thus, the water of the Ivey well at Flomaton contains only 3.8 
parts per million of iron, yet it is very decidedly chalybeate, but the 
total solids in this water amount to only 121.3 parts per million. 
The water of Chandler's spring containing 319.8 total solids and 4.3 
iron, is also chalybeate. The water of the Mentone spring is strong- 
ly chalybeate with 6.6 parts per million of iron and 80.5 parts per 
million total solids. 



326 Chemistry and Classification of Alabama Waters. 

tic medicinal proprieties, that the name "chalybeate" is' com- 
monly applied. In the sediments free from organic matter the 
iron exists in the ferric or highly oxidized condition which is 
insoluble in meteoric waters, but by the action of decomposing 
organic matter this oxide is reduced to the ferrous, which is 
easily soluble in carbonated waters. On exposure to the air 
the escape of the carbon dioxide is followed by the oxidation 
of the iron back to the ferric or insoluble condition, and its 
consequent deposition as hydrated ferric oxide in the run-off 
of the spring. 

"Sulphur" waters are characterized by the presence of sul- 
phuretted hydrogen in such quantity as to give a distinct char- 
acter to the water. The origin, at least of all the Alabama wa- 
ters of this nature, may be traced to the reducing action of de- 
composing organic mater upon sulphates. In very many cases 
this reaction may be very intimately associated with oxidation 
of the metallic sulphides, principally iron pyrites. This oxi- 
dation gives rise to the sulphate of iron and by subsequent 
reactions to> the sulphates of magnesium, calcium, etc. When 
the decaying organic matter is present in sufficient amount 
these sulphates may be reduced to sulphides which may be taken 
directly into solution or by reaction with alkaline waters may 
form hydrogen sulphide. Brines containing small amounts of 
sulphates are liable to contain traces of sulphuretted hydro- 
gen if organic matter be present. 

CLASSIFICATION. 

A systematic arrangement is the first requisite in a study of 
mineral waters'. Any classification, while to- a certain extent 
arbitrary, must be broad enough to include any 'mineral water 
which may hereafter be analyzed and must also be in line with 
modern research. Many classifications have been proposed, 
but the one brought out by Messrs. Haywod and Smith in a 
recent government publication* is the most satisfactory since 
it is based entirely upon the chemical composition of the water, 
the subdivisions being determined by the predominance of one 
or more of the ingredients. The classes are defined not upon 



*Haywood and Smith, "Mineral Water of the United States," Bull. 
91, Bureau of Chemistry, U. S. Department of Agriculture. 



Classification. 327 

the basis of the combinations of the ions* present, as most wri- 
ters have done, but upon the basis of the ions themselves, no 
chemical methods being- known by which in solutions' the rela- 
tive amounts of acid and basic ions entering into combination 
with each other to form salts can be determined. 

In the first place, all waters are characterized by their tem- 
perature and are divided into two great groups : Thermal and 
non-thermal, waters having a temperature above 70°F., being 
considered as thermal. These two groups are treated precisely 
alike so far as their solid constituents are concerned. Each 
contains four main classes : alkaline, alkaline-saline, saline, 
and acid, each of which may be further characterized by its 
predominant acid constituent as carbonated or bi carbonated, 
borated, or silicated for the alkaline class ; sulphated, muriated 
or nitrated for the alkaline-saline and saline classes ; and as 
sulphated or muriated for the acid class. 

If any basic element is prominent in the water this fact may 
be indicated by prefixing its name, (sodic, lithic, potassic, calcic, 
magnesic, ferruginous, or aluminic) to the regular class name. 

If any basic or acid constituent is prominent therapeutically 
but not chemically, this fact may be indicated by adding or 
affixing its name (arsenic, bromic, iodic, boric, siliceous, fer- 
ruginous, etc.) to the regular class name. 

Lastly, any water belonging to any subdivision of either of 
the four classes, may be characterized by the presence of gase- 
ous constituents, as carbon dioxated, sulphuretted, carburetted, 
etc. 

This classification, as to group, class, and subclass, is shown 
in the table below, any class being capable of additional char- 
acterization by naming its prominent acid or basic constituent, 
as above indicated. 



♦According to the modern theories of electrolytic dissociation an 
ion is an electrically charged simple atom or group of atoms forming 
in itself a complete individual, i. e. acting as a chemical unit. To 
illustrate; common salt — sodium chloride — consists of an atom of 
sodium (Na) combined with an atom of chlorine (CI). In solution 
the ions of common salt would be Na for the basic element and CI 
for the acid. In calcium sulphate, a combination of calcium with sul- 
phuric acid, the ions are Ca for the calcium base, and SCm for the 
acid group. 



328 Chemistry and Classification of Alabama Waters, 
scheme of classification. 

Group. Class. Subclass. 

f Carbonated or 

1 1. Alkaline J bicarbonated. 

] Borated. 
[ Silicated. 



Muriated. 

Thermal jH. Alkaline-saline J Sulphated. 

or / ( Nitrated. 

Nonthermal 

Muriated. 

III. Saline__ \ Sulphated. 

Nitrated. 

IV. Acid__ I Muriated. 

(^ Sulphated. 

Alkaline maters. — Alkaline waters are defined as those givinp- 
an alkaline reaction* and containing carbonic or bicarbonic acid 
ions in predominating quantities, and those giving an alkaline 
reaction and containing boric or silicic acid ions in predominat- 
ing quantities, where it can be proved that the alkalinity is due 
to the presence of borates or silicates. 

Saline waters. — Saline waters are those which have an alka- 
line or neutral reaction and contain sulphuric, hydrochloric, 
or nitric acid ions in predominating quantities. 

Alkaline-saline waters. — Alkaline-saline waters lie between 
the alkaline and saline classes. They have an alkaline reaction 
and contain acid ions from both these classes in approximate!}' 
equal amounts. 

Acid waters. — Acid waters are those which have an acid 
reaction, and contain either sulphuric or muriatic acid ions in 
predominating quantities. 

ALKALINE WATERS. 

Tables I and II. 

Of the alkaline waters as' defined above our present inves- 
tigations are concerned with the carbonated only, divisible into 
two groups, one in which calcium is the predominating basic 

*When acid or alkaline reactions are mentioned in these defini- 
tions, methyl orange is supposed to be used as indicator. (Haywood 
and Smith.) 



Classification: Alkaline Waters. 329 

constituent, and the other in which sodium is predominant. 
In only one of the alkaline .waters analyzed did the water fall 
outside of these two groups. The water referred to is that from 
the mineral spring at Citronelle, Mobile County, in which iron 
predominates over all other basic constituents. In the exami- 
nation of these analyses (Tables I. and II.) it will be seen that 
in both groups the amount of mineral matter present is rela- 
tively small, seldom exceeding 300 parts per million. To this, 
however, the water from the Demopolis City wells, with 95 1 . ^ 
parts per million of solid matters, mainly sodium carbonate, 
is a very notable exception. 

These waters are all good for domestic purposes, many < i" 
them constituting the water supply of our cities, and it is proba- 
ble that when more analyses shall have been made, this suit- 
ability of the alkaline w'aters for city supplies will be still more 
clearly shown. 

Table I includes those alkaline bicarbonated waters in which 
calcium is the predominant basic constituent, and of these we 
have 37 analyses, which we place in three groups'; (1) the 
normal calcic bicarbonated alkaline waters; (2) those in wh'ch 
the proportion of magnesium is exceptionallv high, and ( 3 ) 
those in which iron is a characteristic or predominant constitu- 
ent. 

Of the normal waters of group 1, we have 26 analyses, 18 of 
which are of spring waters, 1 of a shallow well, 1 of a river 
furnishing a city supply, and 6 of deep wells. Ten of the 
spring waters, and the shallow (Ingram) well water, are con- 
sidered medicinal waters. The Cold Spring at Blount Springs 
and the Freestone spring at the Alabama White Sulphur 
Springs may be taken as typical limestone spring waters, 
which issue so abundantly from the subcarboniferous limestones 
and from the Knox Dolomite. The Cahaba river water also 
gets its' character from the limestones over which the river 
flows in the upper part of its course. 

Of the 6 deep well waters, three, viz.. those from C. C. 
Ferrill's and the City wells at Selma, and from the well at 
Williford's Landing, contain relatively high percentages of 
the chloride and sulphate of sodium, which brings them into 
close relation with the waters included in Table II. 

In group 2 of Table I, we have placed those bicarbonated 
alkaline waters which are characterized by relatively high pro- 



3S0 Chemistry and Classification of Alabama Waters. 

portion of the salts of magnesium. It is of interest to note that 
of the six analyses here included, five are of "mineral" springs, 
and one of a deep well in the Coal Measures. All the mineral 
springs are places of resort. While in all these magnesic wa- 
ters the bicarbonates predominate, yet the saline constituents, 
chlorides and sulphates, are also relatively abundant. 

Of the chalybeate waters of group 3, one is from a spring, 
one from a shallow well, and three from deep wells. In this 
connection it is to be remarked that the magnesic mineral 
spring waters of the preceding group 2, are also strongly chaly- 
beate. 

In Table II, which includes those bicarbonated alkaline wa- 
ters in which sodium is the predominating constituent, there 
are 17 analyses. Of these, 13 are of waters from deep wells 
coming frOm or through limestone formations, the other 4 
are from springs, three of which are classed as mineral (me- 
dicinal) springs. One of these, the Cherokee spring at Cit- 
ronelle, is remarkable from the fact that the iron predominates 
over all the other basic ingredients of the water. Nearly inter- 
mediate between this class and the preceding are the two deep 
well waters above alluded to, from Selma and from Williford's 
(Table I.) which might with almost equal propriety be put 
in Table II. With the exception of the Exchange Hotel and 
Demopolis waters', the high percentage of sodium in the deep 
well waters derived from limestone formations, appears to be 
due in part to the common salt and sodium sulphate which 
those formations, as marine sediments, normally contain. With 
increase in the relative proportion of sodium salts these waters' 
grade into the alkaline-saline muriated, and saline muriated wa- 
ters which may be considered the typical deep well waters. 

It will be seen by reference to the other tables that about 
half of the "mineral" waters of which we have analyses, are 
included in the bicarbonated alkaline classes', and of these a 
very large proportion, four-fifths or more, contain calcium as 
the predominating constituent. 

It is to be remarked that either of these groups of alkaline 
waters may become chalybeate through the intervention of de- 
caying organic matters, such as are found in the black shales 
of the Paleozoic formations. 

The same black, shales', in conjunction with the oxidation 
products of iron pyrites, a mineral of frequent, almost univer- 



Classification: Alkaline-Saline Waters. 331 

sal occurrence in such shales, are the source of many of the 
sulphuretted waters of this section. The Cook springs in the 
Coal Measures and the two St. Clair Sulphur springs in the 
Cambrian Flatwoods owe their existence to black pyritous 
shales. 

Chalybeate waters are more commonly spring waters than 
deep well waters. The only strongly chalybeate well waters 
in this class are those from the Akron and Brantley wells. The: 
other chalybeate waters' come from springs in the crystalline 
rocks. (Chandler's and Chambers') ; in the Subcarbonifero'.is 
or Mississippian series, (Harrell's) ; in the Coal Measures or 
Pennsylvanian series (Cooks) ; and in the Grand Gulf, (Citro- 
nelle.) 

With the exception of Harrell's' (shallow well), these arc 
places of resort. 

ALKALINE-SALINE WATERS. 
Table III. 

As the name indicates, these waters are intermediate be- 
tween the alkaline and saline classes and contain approximate!}' 
equal portions of the carbonates which are characteristic of the 
alkaline class and of the chlorides and sulphates' predominant 
in the saline class. They are further subdivided into two 
groups, muriated and sulphated, according to the preponderance 
of the chlorides or sulphates which they have derived from the 
strata through which they have passed. 

In this clas's the mineral contents are generally much higher 
than in the alkaline class, and since marine sediments which 
make up the bulk of our stratified rocks are richer in chlorides, 
mainly common salt, than in sulphates, the muriated waters 
hold a larger proportion of mineral matters than do the sul- 
phated. This may be seen by inspection of the table. The small 
amount of sulphates in the muriated waters is also worthy of 
notice. 

In the muriated group of alkaline-saline waters we have 16 
analyses available ; 10 from deep wells, i from a shallow well, 
and 5 from "mineral" springs. Eight of the deep wells, viz., 
those in Hale, Greene, and Marengo counties', and the Pitts- 
boro well derive their waters from the Eutaw sands, while the 



332 Chemistry and Classification oe Alabama Waters. 

Bayou Labatre and Alabama Port wells of Mobile county find 
their water in Miocene or some later Tertiary strata. The 
three sulphur waters of Blount Springs owe their content of 
sulphur to the oxidation of pyrite and the ' reducing action of 
organic matter in the Devonian black shale. The Blount waters 
are generally considered to> be the strongest sulphur waters' in 
the State, a claim which is borne out, so far as the analyses pre- 
sented in the tables accompanying this paper are concerned. :;; 
Only one of the waters of this group is notably chalybeate, viz., 
that from a shallow well of J. W. Bright in Mobile county. 

Of the sulphated group there are n analys'es available, of 
which 7 are of spring waters ; 2 of shallow wells, (Hawkins and 
Beavers) ; and 2 of deep wells, that at Enterprise deriving its 
water probably from the Nanafalia formation, and that at 
Evans Station, from the Eutaw sands. Only one of this 
group is a chalybeate water, the Mentone on Lookout Moun- 
tain, (Coal Measures.) 

In both groups' of this class, the gradual increase of the chlo- 
rides and sulphates present, marks a gradual transition into 
the saline class. 

SALINE WATERS. 
Table IV. 

Under this heading are included two very distinct groups, 
both as regards origin and composition. The one group is char- 
acterized by the predominance of chlorine ions', the other by the 
predominance oi sulphuric acid ions. Both groups contain 
variable but relatively small quantities of carbonic acid ions as 
a result of intermingling with waters of other classes. 

The muriated waters of this class contain as their chief con- 
stituent, common salt, with or without the chlorides o<f potas- 
sium, magnesium, or calcium. Sulphates are practically absent 
(as in the muriated group of the alkaline-saline class), and 
this, in connection with the presence of calcium and magnesium 
salts (chlorides) in relatively large proportion, is' considered 
to be characteristic of ancient brines as distinguished from the 

*The large figure for the sulphuretted hydrogen, (539.2 parts per 
million) in the analysis of Talladega Springs water, given in Table 
IV, is evidently a mistake, since a recent determination made at the 
spring by Mr. Hodges, gave only 19 parts per million. 



Classification: Saline Waters. 333 

waters of modern seas. Their composition points thus to their 
derivation from the brines and mother liquors of ancient seas, 
or from the salts of these ancient seas left in solid form upon 
evaporation of isolated basins. 

Of these muriated waters we have 13 analyses; all, with the. 
exception of a spring situated on the coast in Mobile county, 
from deep wells deriving their supply from a great variety of 
geological formations. The two wells at Holt and the Hosiery 
Mill well at Tuscaloosa derive their water from the strata 
of the Coal Measures ; the Allen well, the Eutaw Dump well, 
the Livingston and the Allison wells, from the Tuscaloosa and 
Eutaw sands of the Cretaceous : the Clarke county salt well, 
from the middle Eocene ; the Jackson well and the Cullom 
Springs well, from the lower Eocene, although the drilling in 
the latter well went clown into the Cretaceous ; the Fort Gaines 
well and the Mobile Oil Mill well, from the Miocene or some 
later Tertiary formation. 

Some of these waters are used for domestic purposes, others 
are too salty for constant use, while the water from the Clarke 
county brine well has been used in the manufacture of salt. 

The waters from the Hosiery Mill well in Tuscaloosa and 
from the Livingston well are considered to have medicinal 
value. The same is true also of the sulphur well at Jackson in 
Clarke county, which yields the only sulphuretted water of 
this class of which we have an analysis'. This is primarily a 
saline water containing a small amount of sulphates, from the 
reduction of which by the organic matters in the water, the 
sulphuretted hydrogen has originated. To the taste this \s 
one of the most pleasant of the mineral waters of the State. 

Of the sulphated waters' of the saline class we have 12 anal- 
yses ; 2 of springs, 7 of shallow wells, and 3 of deep wells. 

The sulphated saline w T aters are of two^-fold origin ; first, 
those formed by the solution of the sulphates existing in the 
strata as' deposits of sulphate of sodium, potassium, magnesium 
or calcium. The calcium sulphate (gypsum) is always pres- 
ent, and it may be that the other sulphates have been formed 
by the decomposition of the gypsum by solutions containing 



334 Chemistry and Classification of Alabama Waters. 

the alkaline and magnesian salts.* Second, those formed by 
the action of the sulphuric acid or the acid sulphates' upon al- 
kaline solutions or upon calcareous or magnesian rocks. The 
sulphated saline waters thus produced through the agency of 
the oxidation products of pyrites must necessarily be of super- 
ficial and local character. These waters', with two exceptions, 
Hightowers and Sanaquat, contain notable amounts of carbo- 
nates, as a result of mixtures with alkaline waters. The sul- 
phated salines fall naturally into three classes according as 
sodium, calcium, or magnesium is the predominating basic 
constituent, and in the greater number of the waters of this 
group analyzed calcium predominates. Several* waters of the 
sulphated saline class contain notable amounts of iron and 
might be called chalybeate. 

ACID WATERS. 

Table V. 

The acid waters of Alabama are due to reactions in which 
the oxidation products of metallic sulphides, mainly iron pyrites, 
take an essential part. By this' oxidation there is produced 
first the sulphate of iron (possibly free sulphuric acid), and, 
by further reactions of this with aluminous, calcareous and 
magnesian rocks, and alkaline solutions, the other sulphates. 
So long as there is an exces's" of free acid or of the acid sul- 
phates of iron and aluminum, the waters will be acid, but by 
progressive saturation of the acid with the various bases men- 
tioned, there will be a gradual formation of neutral sulphates 

*The fact that these waters, with the exception of Perry's, Hard- 
enbergh's and Sanaqua come from springs or shallow wells is full 
of significance. The water standing in these wells has time to take 
in from the surrounding clays, into which the wells have mostly been 
sunk, all the soluble salts within its reach, such as sulphates of 
magnesium, sodium, and calcium, bituminous matters, and if pyrites 
be present, the products of its oxidation and their alterations. The 
Hightower, Mills, and Altman wells, are in the black clays of the 
Flatwoods, while the conditions about the Gary and Jones springs 
and the Tidmore, McGraw, and Landers wells are quite similar, 
though the geological .formations are different. 

-jThe Sanaqua water might probably better be classed with the 
acid waters since carbonates are practically absent. In the very 
high percentage of chlorides, however, it differs from the other acid 
waters which we have analyzed. 



classification: acid waters. 335 

and thus a gradation into the sulphated division of the saline 
waters. These waters', as well as those of the sulphated saline 
class of similar origin, are of superficial and local character. 
These acid waters are, of course, highly medicinal and there- 
fore of much interest. The first from a shallow well of Mr. 
W. E. Forman, is remarkable for the large amount of manga- 
nese sulphate which it holds. The two free acid waters, Dr. 
Hale's and the Matchless Mineral Water of Greenville, are of 
special interest. If we compare Dr. Hale's with the other three- 
waters of the same (Flatwoods) formation, viz.. Hightower'. 1 -; 
Mills', and Altman's, of the saline class, several important rela- 
tions will appear. The Hale water being strongly acid contains, 
of course, no carbonates, the Hightower water similarly has 
practically no carbonates, but also no free acid — the neutrali- 
zation being complete and as yet no accession of carbonates 
from contact with alkaline w r aters. The other two waters, 
Mills' and Altman's, exhibit the further alteration of such a 
water as the Hightower after neutralization of the acid, through 
gradual accession of carbonates by intermingling with ordinary 
calcareous alkaline waters. All three, Hightower, Mills, and 
Altman, seem to betray their derivation from a water of the 
Hale type by their high content of iron diminishing as the 
alteration progresses. 

The other acid water, from the Roper well near Greenville, 
"Matchless Mineral Water," has much reputation as a medici- 
nal water, which it well deserves. I give in addition to Mr. 
Hodges' analysis of the water from a sample taken after a long 
wet seas'on, one by myself and Mr. J. B. Little made many 
years ago, and one by Dr. Metz of New Orleans, to show not 
only the difference in the concentration, but also' in the com- 
position of the water at different times. One analysis shows 
3,615.7 parts per million, another 9,354.4 parts per million, 
over twice as much, and the other 21.490.8 parts per million 
nearlv six times as much. In the dilute water (Hodges' anal- 
ysis) the amounts of chlorine, sodium, potassium, calcium, 
aluminum, and silica are relatively much greater than in the 
more concentrated waters of the other two analyses. On the 
other hand the iron and sulphuric acid ions in the concentrated 
waters are present in relativeh much larger proportion than 
in the dilute. 



336 Chemistry and Classification of Alabama Waters. 



GENERALIZATIONS. 

From a study of the composition of the waters of Alabama 
as indicated by the analyses given in this report, I think we 
may be justified in drawing a few general conclusions, realizing 
fully, however, that entirely reliable generalizations cannot be 
made from a small number of analyses. For the present also, 
we shall consider only the deep wells, leaving the shallow wells 
and springs for a later occasion. 

In the three tables which follow we have brought together 
the analyses' of the deep well waters which, as nearly as we can 
decide it, come from the same geological formation. The class 
to which each water belongs is shown by the Roman numerals. 
The geographical distribution of the wells has also been kept 
in mind in the arrangement of the analyses in the tables, and 
the depths of the wells are given in most cases. In a few in- 
stances' the figures indicate the depth from which the water 
supply comes rather than the actual depth of the boring. 

waters from the Tuscaloosa strata. 

Table VI. 

In Table VI are 13 analyses of waters derived from the Tus- 
caloosa formation. With the single exception of T. B. Allen'c, 
they are of the alkaline bicarbonated class, with relatively small 
amounts of mineral matters and therefore all eminently fit for 
drinking and domestic uses ; the exception is a strongly saline 
water due to the presence of a large amount of salt. 

The waters from the McLendon well, the Union Springs 
Water Works, the Prattville Academy, and the Exchange 
Hotel, all from East Alabama, and the Demopolis well in Wes- 
tern Alabama, belong to the subclass in which the sodium pre- 
dominates over the calcium, and this predominance is due to 
the presence of bicarbonate of sodium rather than to common 
salt, sodium chloride. The waters from the Elliott and the 
Auxford wells near the Tombigbee river in Hale and Tusca- 
loosa counties, are clearly of the subclass of alkaline waters 
in which the calcium predominates. The waters from the two 
Akron wells might be put in either class, since the proportions 



Generalizations: Deep Well Waters, 337 

of sodium and calcium are approximately equal. The two 
Selma waters, and that from Williford's Landing are, in a way, 
intermediate between the two subclasses, for while the calcium 
predominates in each, the amount of sodium is quite high, 
and the large proportion of chlorine, especially in the Williford 
water, seems to show that this is due in part at least to com- 
mon salt. 

From the analyses above presented it appears that from the 
meridian of Montgomery eastward, as a rule, these waters 
are characterized by predominance of sodium salts, chiefly so- 
dium bi-carbonate. To the westward of the Montgomery me- 
ridian the subclass with predominant calcium salts (bicarbo- 
nate), is more frequently represented, not however, to the ex- 
clusion of the sodium subclass, as may be seen in the analyses 
of the Demopolis and Akron waters.' Furthermore the propor- 
tion of common salt seems to be greater in the waters wesc 
of Montgomery than in those to the east. But the great excess 
of salt in the water from T. B. Allen's well is remarkable, con- 
sidering its source in the Tuscaloosa sands. 

By way of a partial explanation of the facts brought out, \t 
may be stated that the Tuscaloosa formation, being in the mam 
if not altogether of fresh water origin, would naturally contain 
only a small amount of common salt in its strata. And since 
the materials of this formation in east Alabama were probably 
furnished by the disintegration products of the igneous and 
metamorphic rocks, while in west Alabama they were provided 
by the sedimentary strata of the Coal Measures and other Paleo- 
zoic (marine) formations, the prevalence of the sodic subclass 
in the eastern section and of the calcic subclass, especially when 
notable amount of common sail is present, in the other section, 
may be accounted for. 

WATERS FROM THE EUTAW SANDS 
Table VII. 

In Table VII are assembled the analyses of waters from the 
Eutaw sands'. Of the 16 analyses here included, practically all 
belong to the saline and alkaline-saline classes, mainly the lat- 
ter. The two which are assigned to the bicarbonated class 
with predominance of sodium, viz. Wedgworth's and Madi- 
son Jones', contain so much salt, as indicated by the relatively 

22 ~ 



338 Chemistry and Classification of Alabama Waters. 

high chlorine content, that they might almost be included in the 
alkaline-saline class. While all these waters contain large 
amounts of common salt and are therefore to be classed as 
muriated, yet three of them, viz., those from the Perry well in 
Russell county, and from the Evans and Hardenberg wells in 
Hale county, contain so much sulphate of lime as to bring them 
into the sulphated division. In every other case the amount of 
sulphates' is exceedingly small, sometimes dwindling to a mere 
trace or to practical absence. They all contain notable amounts 
of carbonates. 

These facts find their explanation in the circumstance that the 
Eutaw sands are marine sediments and contain the salts of the 
ancient seas in which they were deposited. While the carbo- 
nates are chiefly carbonates of lime and magnesia leached from 
the limestones interstratified with the Eutaw sands, yet in the 
majority of cases the alkaline (potassium and sodium) car- 
bonates are also present in these waters. 

WATERS FROM UPPER CRETACEOUS AND TERTIARY STRATA. 

Table VIII. 

In Table VIII we have five analyses' of deep well waters de- 
rived from the Upper Cretaceous or Blue Marl strata of east 
Alabama, and n of waters derived from several horizons of 
the Tertiary. 

Blue Marl Waters. 

The five analyses under this head belong to the Alkaline 
b'icarbonated class with predominance of sodium salts, and arc 
all, with the exception of the Andalusia well, from wells in 
Barbour county. By referring to the first four analyses of 
Table VI, which are also of waters from East Alabama wells, 
it will be seen that they belong to* the same class of sodic alka- 
line bicarbonated water, although derived from a different for- 
mation — the Tuscaloosa. 

The waters of the Clayton City supply, and from the Comer- 
Bishop and C. H. Bishop wells, are practically identical in com- 
position and come from approximately the same horizon. In 
these the sulphates are slightly in excess of the chlorides, as is 
the case also with the water of the Union Springs City supply 



Generalizations: Deep Well Waters. 339 

given in Table VI. In the other two, Andalusia and Moul- 
throp's, the chlorides predominate slightly, but in all five the 
carbonates' (mainly of sodium) are considerably in excess of 
other salts combined. A somewhat similar relation is charac- 
teristic also of the four waters of the Tuscaloosa formation 
(Table VI) above referred to. 

It would seem reasonable to offer the same explanation of 
the predominance of the alkaline (sodium) carbonates in the 
Blue Marl waters as was' suggested for the Tuscaloosa-derHed 
waters of these eastern counties, viz., the formation of the sed- 
iments from the decomposition products of the near-by igneous 
and metamorphic rocks. The relatively larger proportion of 
chlorides and sulphates in the Blue Marl as compared with the 
Tuscaloosa waters, accords with the marine origin of the Blue 
Marl strata. 

Tertiary Waters. 

The 1 1 analyses of waters from Tertiary strata are arranged 
in geographical order from the coast regions of Mobile county 
northward and eastward. The Mobile county wells and the 
Ivey well at Flomaton derive their supply from the middle or 
upper Tertiary strata, (Miocene or Pliocene). The Mobile 
county wells all yield salt water, (muriated alkaline-saline and 
saline.) The water of the Ivey well is sodic Alkaline bicarbo- 
nated with enough iron to> make it decidedly chalybeate. The 
water from the town well at Brantley in Crenshaw county, is 
quite similar, but in it the calcium predominates; it also is 
strongly chalybeate. 

Of the three salt wells, the two in Clarke county, viz., the 
Brine well and the Jackson sulphur well, probably get the salt 
water from the Hatchetigbee formation ; in the Cullom Springs 
well in Choctaw county, while the boring went down well into 
the Cretaceous, the main stream of salt water is from a depth 
of about 800 feet and therefore probably from the Nanafalia 
formation or the next underlying Naheola. 

All the salt wells and salt oozes of Washington and Clarke 
counties seem to be in some way connected with the Hatchetig- 
bee and Jackson anticlinal uplifts, and while in many places 
along the flanks of these anticlinals, especially along the South- 
ern flank of the Hatchetio-bee, the salt water comes to the 



340 Chemistry and Classification of Alabama Waters. 

surface in oozes or springs, or is brought to- the surface by bor- 
ings ranging in depth from a few feet to 300 or 400, it may be 
that its real source is in deeper lying strata, and that its occur- 
rence at the surface and at shallow depths may be due to arte- 
sion conditions in the inclined strata of the uplifts and the exis- 
tence of cracks or the locally porous nature o<f the overlying con- 
fining strata. The town well at Enterprise probably draws upon 
the Nanafalia sands for its supply, and in its relatively small 
amount of dissolved solids, the sulphates are slightly predomi- 
nant over the carbonates. The deep borings of the Ozark City 
water works will probably reach the lower strata of the Tertiary . 
For a deep well this water is of rather exceptional character, be- 
ing a normal calcic alkaline bicarbonated water, and more like a 
spring or shallow well water than a deep well water. This 
composition and the relatively small amount of dissolved solids 
insures its suitability for a city supply. 

We have as yet too few analyses of waters from the Tertiary 
deep wells to justify any serious attempt at a geological or geo- 
graphical classification. 

From this comparison of the analyses of the bored well waters 
derived from the three Cretaceous formations we are led to 
the following conclusions ; ( 1 ) The strata of the Tuscaloosa and 
of the Blue Marl or Ripley formations yield waters of the al- 
kaline class, which includes the waters best suited for domestic 
use. The waters from the Tuscaloosa as a rule, do not hold 
more than 200 to 250 parts per million of solids, while those 
from the Blue Marl hold in general between 350 and 400 parts. 

In all the Blue Marl waters, and in those from the Tusca- 
loosa east of Montgomery, the sodium predominates over the 
calcium, while in the Tuscaloosa waters westward from Mont- 
gomery, as a rule, the calcium is predominant. The larger 
proportion of total solids in the Blue Marl waters seems to be 
due to a relatively larger proportion of the sulphates and 
chlorides, the proportion of carbonates in these and the Tusca- 
loosa waters being approximately the same. 

(2) The waters from the Eutaw sands are more highly 
charged with mineral matters' than those from the other two 
formations, the total solids ranging on an average from 400 to 
5000 parts' per million. 

Of the dissolved mineral matters, common salt (sodium chlo- 
ride) is usually the most important and characteristic, although 



Generalizations : Deep Well Waters. 341 

in two of the analyses the sulphates are in excess. Because 
of this high percentage of salt most of these waters fall into 
the alkaline-saline and saline classes. Even in the two waters 
in which the carbonates predominate the proportion of salt is 
notable. While by reason of the large amount of dissolved 
solids which they contain, the waters from the Eutaw sands' 
are not so well suited for domestic purposes as those from the 
other formations, yet they are very extensively so used in the 
"prairie" or "Black belt", where the surface waters are defi- 
cient. By far the greater part of the bored wells' of which wo 
have records are in this prairie belt and derive their supply 
from the underlying Eutaw sands. 

The following extracts with accompanying sketch map, taken 
from the Report of the Alabama Coastal Plain, pages 306 and 
307, may possibly throw some light upon the relations of the 
Cretaceous formations which have been instrumental in causing 
these differences in the waters from the different formations and 
from the geographically different parts of the same formation. 
It must be borne in mind that the Tuscaloosa formation is of 
fresh water origin while the ethers are, prevalently at least, 
marine. 



842 Chemistry and Classification of Alabama Waters. 




Distribution <>f Cretaceous Formations. 343 

"An examination of the distribution of the Cretaceous for- 
mations in the adjoining states will make the condition of 
things in Alabama more easily understood, and for this' purpose 
the accompanying sketch map has been prepared, Plate XVI. 
Of all the Cretaceous formations the Tuscaloosa is the most 
widely distributed. It continues eastward along the foot hills 
of the Appalachians to Maryland and beyond. The other divi- 
sions have not been traced eastward beyond the western part 
of Georgia. The map will show how in the upper half of Ten- 
nessee the whole Cretaceous, above the Tuscaloosa, is repre- 
sented by littoral or offshore deposits, chiefly sandy, in which 
there are a few fossils of Eutaw species' in the eastern or 
lower part, and of Ripley species in the western. In the eas- 
tern part of Alabama we have a similar state of things, for 
along the Chattahoochee River the lower parts of these sandy 
strata hold Eutaw species' and the rest Ripley species, all the 
strata being of littoral or off-shore character. Below the cen- 
tral line in Tennessee the chalky beds of the Rotten Limestone 
wedge in between these two sandy series and gradually narrow 
down or crowd out the upper or Ripley portion of them, so 
there is a good stretch of county in northeastern Mississippi 
where the chalky strata represent the entire series above the 
Eutaw sands, and border upon the Tertiary formations, in di- 
rect contradistinction to what we have seen in northern Ten- 
nessee and eastern Alabama, where beds' of the Ripley aspect 
represent the entire series above the Eutaw. In Sumter county, 
Alabama, or perhaps in the immediately adjacent parts of Miss- 
issippi, the Ripley beds set in again as a margin of the chalk 
area, at first narrow, but widening out towards the east, until 
beyond Macon county, Alabama, it represents the whole upper 
series as above stated. From this we may also infer a good 
deal concerning the conditions which prevailed during the dep- 
osition of these Cretaceous beds, for we see that in the central 
part of this area, extending from Macon county, Alabama, 
around to the central part of Tennessee, deep or open sea pre- 
vailed during the greater part of the upper Cretaceous 
times, while contemporaneously, in the eastern part of Ala- 
bama and the northern part of Tennessee shallow water or off- 
shores deposits were accumulating." 



344 Chemistry and Classification of Alabama Waters. 



CONCLUDING REMARKS. 

An extended discussion of mineral waters from the point of 
view of their therapeutic, or curative action upon the human 
system, would be foreign to the intent of this report, which 
is to give a general account of the underground waters of Ala- 
bama. It is hoped, however, that the mineral waters with which 
our State of Alabama abounds, may be considered later in a 
special report, after fuller investigations and more numerous 
analyses. 

A few words may nevertheless' be appropriate here concern- 
ing the chemical relations of potable and mineral waters, and 
sanitary and unsanitary waters, and concerning the limitations 
of a chemical analysis in discriminating bet wen them. 

The characteristics of a good drinking water have been de- 
fined as follows': (i) It should be clear and limpid. (2) It 
should be colorless. (3) It should be odorless, especially free 
from sulphuretted hydrogen or putrefactive animal matter. (4) 
It should be cool. (5) It should have an agreeable taste : neither 
flat, nor salty, nor sweetish. (6) It should be free from dis- 
ease germs, (7) It should be free from all other substances 
mineral or organic, injurious to the human system; especially 
from dissolved organic matter o<f animal origin. (8) While 
a certain amount of saline matter is necessary to give the water 
a good taste, the total amount cf dissolved solids should not as 
a rule exceed 500 or 600 parts per million, including not more 
than 30 or 40 parts per million of chlorine. A certain amount 
of gases', consisting of carbon dioxide and air (oxygen and 
nitrogen), is also essential to give life to the water and to save 
it from flatness. 

The first five of these are physical characters, determined 
by the appearance, or the smell or the taste, and not by a 
chemical analysis. The sixth and seventh are the characters 
that distinguish a sanitary from an unsanitary water, and these 
are determined either by microscopic examination or by a "san- 
itary" chemical analysis, which is quite a different thing from 
the ordinary mineral analysis. It is therefore only the eighth 
characteristic which falls in the domain of the usual analytical 
methods. 



Sanitary Analysis. 345 

Sanitary Analysis. — No fact has been more clearly demon- 
strated than that diseases may be disseminated by water, and. 
it is equally certain in some cases, and probable in all, that 
these diseases are due to microscopic organisms which flour- 
ish best in solutions of organic matter of animal origin, hence 
the common belief that waters' contaminated by decaying animal 
matters or refuse are most dangerous to health. The micro- 
scopic organisms above referred to may be detected by exami- 
nation with microscope by a competent observer. A number 
of specific disease germs, such as the germ of typhoid fever, 
are well known, and when these are detected in the water there 
can be no question of its unsanitary character. Such exami- 
nations', however, belong to the bacteriologist and not to the 
chemist. 

The nitrogenous animal matters which sustain the life of 
these disease germs, in the process of their decomposition in 
waters, yield "albuminoid" ammonia, (or ammonia from or- 
ganic nitrogen,) and this by further decomposition yields in 
succession nitrons and nitric acids which combine with bases 
present to form nitrites and nitrates respectively. 

The presence, therefore, of certain minimum amounts of al- 
buminoid ammonia (as distinguished from free ammonia or 
ammonia salts), and of nitrites and nitrates may lead to well 
grounded conclusions as to the amount of decomposing (pol- 
luting) organic matter and the stage of the decomposition. 
If only the nitrates are present the inference is that the water, 
if previously contaminated by decaying animal matters, has 
again become pure through their removal by complete decom- 
position. But waters holding a notable amount of organic am- 
monia or of nitrites or of both, would still contain the material 
upon which disease germs thrive, and would therefore be dan- 
gerous to health. 

All natural waters contain some chlorine, but when the 
amount in a potable water exceeds 50 parts per million, the 
suspicion is that this excess is due to the pollution of the water 
by sewage or animal excretions. An inspection of the analyses 
given in the tables above, will show- that the waters from 
many of our deep wells, where there can be no question of 
contamination, contain much more than 50 parts per million 
of chlorine, so* that in considering the amount of chlorine as 
an indication of contamination, the source of the water as well 



346 Chemistry and Classification oe Alabama Waters. 

as the normal chlorine content of the waters of the particular 
district, must be taken into account. In itself, therefore, the 
amount of chlorine in a water is no' evidence of contamination. 

In similar manner the presence of albuminoid ammonia and 
of nitrites in excess of an accepted limit, while it may throw 
suspicion upon the water as to its sanitary character is by 
no means a certain evidence thereof. In fact it is doubtful 
if any purely chemical examination of a water can alwayi 
be relied upon to establish its sanitary or unsanitary character. 
Of course, where these suspicious matters are present in large 
excess, or where even) normally harmless constituents are 
present in quantities like 1,000 or more parts per million, the 
chemical analysis might be conclusive ; as would be the case 
also if among the mineral constituents of the water there were 
found any actively poisonous compounds. 

While there are many who are firm in the belief that the, 
character of a water may be centainly determined by the "san- 
itary analysis" above referred to, some of the most experienced 
investigators of the subject have been forced to the opposite 
conclusion. In a paper on "The Futility of a Sanitary water 
analysis as a test of potability"* Mr. Marshall O. Leighton of 
the United States Geological Survey, contends, and we think 
proves by citation of many analyses, that "the sanitary anal- 
ysis offers nothing by which one may positively distinguish 
between a dangerous and a wholesome water." Dr. William 
M. Drown one of the most eminent of the students of sanitary 
problems, in speaking of the sanitary analysis, is quoted as 
saying :t "My long experience in this line of work has im- 
pressed me with many doubts concerning its value." 

Analysis of Mineral Waters — When we undertake by a 
chemical analysis to determine me mineral or medicinal charac- 
ter of a water we are confronted with difficulties that in some 
cases appear to be insuperable. When the analysis reveals the 
presence in the water of very notable amounts of Epsom or 
Glauber salts, of sulphuretted hydrogen, or iron, or of other 
active medicinal compounds, there is' no difficulty in pronoun- 
cing upon its mineral character or in forming an opinion as 
to the constituents to which the medicinal virtue is due. 

*Reprint from Biological Studies by the Pupils of William Thomp- 
son Sedgwick, Boston 1906, page 36 and following. 
fReprint above quoted, page 48. 



Analysis ok Mineral Waters. 347 

On the other hand there are many springs which have rightly 
acquired great reputation for the curative properties of their 
waters, which upon chemical analysis are found to be not so 
highly mineralized as the majority of potable waters, and to 
contain nothing by which their medicinal character can be ac- 
counted for. Judged by the chemical analysis many of these 
waters would be pronounced exceptionally pure waters' of the 
alkaline bicarbonated or alkaline saline class, often with less 
than ioo parts per million of dissolved mineral matters. 

Man)' analyses of mineral waters are thus a distinct disap- 
pointment to the proprietors of the springs and to the doctors', 
who naturally, in view of the well established curative character 
of the waters, expect the analysis to reveal the presence in 
large amount of some substance of unequivocal therapeutic 
value. , 

These analyses are also sometimes a* source of embarrassment 
to the chemist, as may be inferred from the following extract 
from a letter just received at this office : 

" — , March 6, 1907. 



Dear Sir: — I spent one day this week with at 

He has what he thinks is a very fine mineral 

spring there. He had the water analyzed once, by Mr. R. S. 
Hodges, I believe. He is not quite satisfied with the analysis, 
however, as the doctors say the water produces a greater effect 
than is indicated in the analysis." 

The water in question contains less than 50 parts per million 
of mineral matters, consisting mainly of the carbonate, chlo- 
ride and sulphate of sodium. The proportion of iron is' rela- 
tively large but the calcium and magnesium are in smaller 
amounts. The inference would be that the curative effects of 
the water were due to the presence of the iron salts and the 
sulphate of sodium, but the small amount of mineral matters 
of any kind seems to be the stumbling block. 

In this' connection I cannot perhaps do better than quote 
some of the statements of a distinguished student of the Min- 
eral Waters of the United States.* "A number of the waters 
included, and of importance commercially, would be consid- 

*A. C. Feale. Fourteenth Annual Report of the Director of the U, 
S. Geological Survey, page 57. 



348 Chemistry and Classification of Alabama Waters. 

ered indifferent when viewed in the light of their chemical 
composition, but it must be remembered that some very pure 
waters have an undoubted therapeutical effect, and that chem- 
ical analysis, which is absolutely reliable only in its estimation 
of basic s'alts and acids, will not always explain the medicinal 
effect of a water, and that small quantities of some constitu- 
ents are often more effective as remedial agents than others 
that are present in larger quantities." It might be well also 
to bear in mind that a given amount of a medicinal substance 
taken into the system along with a large amount of water, 
may be quite as' effective as the same amount taken in more 
concentrated form; in other words, that the actual amount in 
parts per million of the ingredients of a mineral water (i. e. 
its concentration), is of less importance than the relative pro- 
portions of these ingredients. 

In the light of recent- discoveries, it seems highly probable 
that the curative effect of some mineral waters' of this kind 
may be due to' the presence of radium or of some radio-active 
substance, which the ordinary chemical analysis does not reveal. 

While the ordinary limit of the amount of total solids in a 
potable water is put at 500 to 600 parts per million, it will be 
easily understod that if the sulphate of sodium, or magnesium, 
or other active medicinal salts, make any considerable propor- 
tion of these total solids, it would unfit the water for constant 
use. Conversely, some waters with a far greater amount of 
total solids' than 600 parts per million, may be used for drink- 
ing purposes if certain substances, notably common salt and 
alkaline carbonates, constitute the major part of these solids. 

Many mineral waters of repute are among the purest of 
potable waters, and some, even if they contain substances of 
active therapeutical value, may be tolerated by the human sys- 
tem and, if the dilution is sufficiently great, may serve as a po- 
table waters. 

Concerning, however, the use of such strong medicinal wa- 
ters as those described under our s'ulphated saline class, some 
comment may not be amiss, and in this connection the words 
of Dr. E. W. Hilgard, in that Loo little known and appreciated, 
but best of all State Reports, the "Agriculture and Geology 
of Mississippi," (p. 286) are quoted : "It cannot be too 
strongly urged upon the inhabitants of these regions * * :!: 
* * * * that the habitual use of mineral water proper of 



Use of Mineral Waters. '349 

any kind, is no more rational than would be the use of any other 
medicine, with persons in a normal state of health. It is often 
said that mineral waters are "Nature's own remedy," which 
may be true enough, provided there is something to be reme- 
died. The Epsom salt, Glauber's salt, etc., contained in these 
waters, are no less purgative, debilitating, and therefore inju- 
rious to persons in good health, than the same articles are 
when derived from the druggist's vials.' 



TABLES OF ANALYSES 

OF 

ALABAMA WATERS 



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23.4 

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29.6 

175.6 

5.7 
2986.1 

3.2 
173.7 

S.7 




d 
10 

rH 

10 


•A^unoo 3>iaBio 
'uos>pi3f 'H9A1 anqd^ng 


8.2 

960.3 

16.0 

54.0 

2.6 
1466.5 

6.4 

267.1 

17.8 

* 


Ci 

Ci 
Cl 


■A":,rjrnoo enqoiAi 'enqow 
at-BU 'naAi s,oo no uouoo 


O; lO rH rH 1 IIO 1 I CO CM I 

id id i> id ! ! © 1 ! rH oi ! 

rH CO rH Tfl 00 rH 
rH ■* CM 
1-1 1 1_l 1 ! 


t- 

rH 

rH 

Ci 
CM 


•A^unoo 'bsooibdsux 
Bsoorvo&nj 'iI9av uiui AViaisou 


OS l> OS © 1C3 | O ,Cjr-;cC | 

id co ■* © ' i cd i ci ci t-i i 

• "* rH t- 1 O 1 I3H 1 

■<* 1 t- 1 rH 1 

1 1 1 

1 1 1 

1 1 1 


CO 

d 

CD 
CO 
rH 


11.8 
295.6 

20.7 
109.8 

1.7 
649.6 

.6 

116.6 

15.9 


CO 
tH 
CM 
CM 

rH 


•Ajunoo jtbh 
'8[ItAiumoH 'tranv 3 '^IL 


■Aiutioo bsooibosuj, '^ioh 
'Z oiv [I8A -oo "I 3> I-BJtTuao 


iHffiHO 1 OIO iptr-;00 1 

ci t> od i-i ! co -h" ! id d d ! 

rH t- CM 00 rH t- CI GO 
T-i ■* J 


CO 

d 


Oi 


Aiimoo 'Bsooi'Bosnx 'IIOH 
X on h«a\. -oo "I 3» -0 IBJ^tiao 


C"| p rH O 1 t-_ CO 1 rH T-j ID IC5 

oo ci r-i th" ! co d ! id rH" id r-i 

>0 CO 00 rH -HH CI t- 
rH Tfl- 


rH 
rH 

rH 
00 


'A^unoo anqojv 

'SiltrVB-Q '},£ 'H9Ai }UaraUJ9A0!3 


4.1 

'125.7 

1.4 

6.1 

1.6 
192.9 

2.0 
29.1 
53.9 


00 

d 

r^ 
tH 


oo snqoiAi 'sa^'Eq'Bq no Aug 
r 'on "ads Sjaqraoag - a\ '£ 


t- t~ Ci CD CO It- 1 tH 1 rH 1 

r-i co ci ! ci ! r-i ! d ! 

! rt ! ■ I ■ I 

i i i i 
i i i i 


t- 

d 

CM 


>> 
Constituent. j 


Potassium (K) _ 

Sodium (Na) 

Magnesium (Mg) _ __ 

Calcium (Ca) _ _ 

Iron (Fe) 

Iron oxide (Fe20s) and 

alumina (AI2O3) 
Chlorine (CI) 
Bromine (Br) 
Sulphuric acid (SO*) 
Bi-Carbonic acid (HCOs) 
Silica (Si0 2 ) 
Hydrogen sulphide (H2S) __ 





359 



a)uuoo uosip^M 'aniAsjunH 


ICO t- *+ t- -f CO 
CM* ■* l- © CO © 


1 CO 

J id 


i q * 


co q 

' CD 35 


rH 

CO 


11 ;A\ .19}T;AY IB.I8UIIU 'BlibBU13S 


(MMCCH 


H 


CD 


05 


rH CO 


rH 




(0 iH ^ 






1 °° 


CO 




rH 




01 








| KO 




© 


__ 














i-H 


CO t-J i-J CO 






C5 Ol 


1 1 it 


X i 


-v 


•Aiunoo aa^rang 


r- lq co t-h 






CD* r-" 


1 CD -t" 


LO ' 


-* 


'.m.ioa 'USAi. mmmv 'V AY 


CO © CM O 

1- t- o 

1 






r-( CD 


CO O 
CC -f 
1 "^ 


1- I 


© 
lO 

t- 


•A^unoo J9} 


05 GO ^ eO 






O CO 


1 -t- CO 


© 1 


© 


rH* 05 ci r* 






t^ - o* 


! co o 


id ! 


© 


-uuis - >IJ0A "IieAi sum d D 


© LO -f CO 

co iro iro 






rH CO 


LO CO 

ico 


iro | 


© 

CD 












co 




lO 




1-0 © CO 01 






01 r-i 


i r q 


r. i 


C5 


■^junoo .laiiuns 'uoi) 


ei © co t> 






CO i-i 


id TjH 


ci ! 


1* 


■T3+S vmQ 'll d/A -i3Avo;qSiH "a 


01 -H CO o 

LO CO CD 






i-l CD 


CO i-l 

o 


-* ] 


I- 












CO 




10 




CD 01 t- b- 






* IO 


-. * 


"id i " 


~© 


•^unoo aa;uins 'sadg 


•V •* I- t- 






LO* 


D5 CO 


■* ! 


I- 


.:U3U 'SuudS G9UOf ,r J U9pj-BH 


l-H I- t- rH 

CO CM © 






CD 

CD 


CO ICO 
O if 
OI 


H j 


© 

iro 




CO CO O 00 






O CO 


Z 10 


OI 1 


1-| 


•A^nrtoo. xoohai 'BiuoparEO 


rH O 03 05 






01 o 


oi co* 


LO 1 


tA 


'ipm AonEqs 'AvejfPM H AA 


l-H LO CO -t 1 






iH 
CO 


i-l CO 
b- CO 

rH 


-H 


© 

co 




CO CO 01 CO 






CO CO 


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■* 1 


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05 


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rH t- 00 1Q 

r- co 






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l-H 


lO , 


iro 

CO 
CO 




t- CO CD r-( 






C5 CO 


'Ti CO l- 


CO | 


rH 


•A}unoo qqia 


cm -i" id co 






CO CO 


t-" CO b- 


CO* 1 


i-i 


'811AJ91U90 'Suiads A.IV*) 


CO 1(0 

T}1 








co oi -1- 

CO r-f 
rH 


i-H 1 


© 
© 
OI 


'A)unoo es^oaeqo ^[^ 


C5 lH CO CD 

id oi co co 






HO CO 
CO t-* 


iro co 
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© 1 
© 1 


rH 


n^a 'iisAs. minis a uqof 


rH 05 O 
r-l CO 






01 


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CO r^ 
rH 


CN ] 


CO 
i-H 
CM 




1 CO 05 CO 






TjH l> 


iro co 


^ I 


rH 


'A^unaa unoqi^o 'eniA 


j r-i CM* CD 






CO 


t>* CO 


id ! 


00 | 


-uos^oBf '[pA\ saapuBq - h 'V 


■* CN t- 

J i-l CM 








^ o 

© 01 


CO j 


LO 
rH 




CO - CD Tl 






Ol tH 


Tt< CO 


-* l 


CO 


•A}unoo ai^H 'ujaq 


-i* CD 05* 05* 






oi c* 


© CO 


CO* 1 


rr 


-A9^ 'II9AV qSjequapa-BH 'S 


01 CD CO CO 
Ol lO 






i-l 01 


CD 01 

t- iro 


"* I 


CO 

05 
CM 


•A}unoo nassiry; •eniAtiai-o 


© OI 1T0 ICO 
CO b-" i-i CD 






CO lO 
T-i CO* 


LO* oi 


"*. ' 


CN 

b-* 


jvqu 'i om U9AV Axia^ q a 


CO CO 






t- 


t- r-i 


rH 1 




•A^ireooq 


1 1 1 1 1 
1 1 1 1 1 

1 1 1 1 1 
1 1 1 1 1 
1 1 1 1 1 
1 1 1 1 I 
1 1 1 1 1 
1 1 1 1 1 
1 l 1 l i 

I 1 1 1 1 

II II 




d 




1 1 1 
1 1 1 
1 


i I 
1 W 

1 d) 




-t-J 


1 ^ ! 




1» 


T ! 


0Q- § 


I 2 




d 




—> 


qo 


^2 "w, 


! 2 




2- 


d 


<u 


r— . 


T3 CJ 


5 




co 
d 
Q 
O 


K ca en ] 

~*aB 
a w d © 

2 d m a fa 
ra -> a — i 


< 

a 


'on oxide (F 
alumina (A 
hlorine (CI) 
romine (Br) 


ulphuric aci 
i-Carbohic a< 
arbonic acid 


^3 

M S 

— >> 






ftMgOM 


^ 


hH 


OH 


Oi mo 


Mffi 





360. 

TABLE V. ACID WATERS, 
b. sulphated. 



Constituent. 



O 



m 

Pi 

n . 

<M" g 

to (h 






n p) 

•eg 

02 






o3 d 



i— h 0) 

s-i a> 

O) cu 

a & 
o ci> 



-w l~> 


>?>; 


•S !-i 


§g 


J,2 


^m 






-^ bi 


.ph 03 






*? 


. pi 


rt .ffl 


^b 


"3 of 


P 5 aT 


£s 


+J 


£* 


%, >i 



ft u 



Potassium (K) 

Sodium (Na) 

Magnesium (Mg) 

Calcium (Ca) . 

Manganese (Mn) 

Iron (Fe-ferrous) 

Iron (Fe-ferric) ■_- -__. 

Aluminum (Al) 

Iron oxide (FeaOs) and 

alumina (AI2O3) 

Chlorine (CI) 

Sulphuric acid (SO*) 

Sulphuric acid-free (H2SO4) 

Bi-Carbonic acid (HCOs) 

Silica (SiO») 



2S.2 
23.8 
26.6 



7.1 

7.9 



276.0 



50.0 



619.6 



1.0 

4.8 
23.0 

65.0 



42.6 
336.0 



55.4 



1.9 

6.9 

37.4 

88.4 



44.6 
32.2 



618.0 



7.1 
34.5 



511.8i 871.0 



14.1! 7.6 15.8 

379.1, 57.6J 51.9 

258.6 78.0 235.1 

315.3 1 322.4 300.8 



86.6; 



90.5 1085.0 
204.1 1038.4 
132.8 33.2 



354.5 1 78.3 
2283.3 : 2493.3 
i 19.9 



92.4| 131,2 



42.3 

6434.8 
30.7 



86.4 



3783.9 3615.7: 9354.4 



33.0 
76.9 

278.0 
373.4 



1358.8 

4013.7 

69.8 



53.2 
15130.3 



103.7 



21490.8 



Trace; percentage not determined. 



:<n 



•oo 8113H 'auiApunoiM 
JB9U 'neAv s ( uanv '9 \L 



•siiiih 'IRAv s,p.iojxnv J, k 



•A^unoo 8IBH '91H A 
punopj; 'H8A\. s^onia 'V f 



•A^UnOO BS00['BDS11J J 

'U9M. SuipuBi s paojnUAV 



oo aii?H 'no.uiv 

3 -ON H9A*. '-oo puBq J3HBA\. 



■X;unoo 81BH 'uojjiv 
I "ON I19M. '«0 Puet aanBAV 



i- f. :i : 

Cl r-l 



*r 35 -t- rq 
ti -r x d 



CO IN lO CO 



q ■* co — 
i- it- i" i cd 

rlH <M 



n to o e a 



"f r-l r-l 



^ I- 



10 O riQQt 

ci i- i~ / i- 



q <n co o 05 

c i -v -r z os 



l~ f * OH 

ci t- d co 



q s; co ci q S3 

co ss' ' oo © T-i 



CO rH CO © q 00 

"# 00 ' t- C o' v-i 



oc ci cc 

d S3 05 



T-j N CO I- 
CO LO GO t~ 



■^unoo ogua.iBH 'sipdora 
■8Q 'si[9M. s^joav .i9}ba\ A.%\o 



ICCHl- I 



C CO * O i-l 



"X}linO0 SBH^Q ''BUI 
-19S 'SH9AV S^JOAY .19}BA1 A}10 



■* O CO CO 

id in" ci © 



•A^unoo sbubq 
"Btuias 'I19A sjnaaa^ o '0 



i~ oi :/: co 



C X CC Lt c 



X f 1" J! x 



•oo a"j9uioSiuoj\[ 'AaaiuoS 

1UOJM 'H9AV I9^0H 9SU'Bipxa 



Cl I h CO * 

d oo ' -j 
1-1 1- 



t- 10 H X 

1- T-i -P T-l 



•A^unoo •eSriBinv 
'eniA^'BJj 'H9Ai AuiepBoy 



Cl CO T CO Cl 



•A^unoo iponng 'sSuudg 

u 0I u fL 'II 9A ^ SJI.IOM. J9}BAY A^JO 



cq ** ci iq 

d ri ' Cl 



•A^unoo jp ssn H '99R0IA 
■so 'IRav s t uopueT[oi\[ T AV 



oq © t-- ia 

r-I CO ' r-i 



I- -1J 00 00 rrf 

'fflri-t id 
OO Cl r-l 



q i- -* iq oq 
ci ri d co d 



•A^BOoq 



~0 



-s 



*ifc 



P-i 02 



■a a 

CD H 

a -S 

M « 

So 



03 4i 






Cl a 



c S c c o »-? 

o 2 g - 3 3 S 



03 
P 



362 



A^unoo 
e£ua.rej\[ 'uapuiq 'udJA oiiqna: 



•^unoo ja^inng 'A'ui'cngg 
'l\Qi&. s/oo jgqranq uosinv 



•a^utioo aainins 



t- CO CO CM 



■r. 



i 10 \n 
! t- d 



550.0 
1.6 

7.2 


OH 

id id 

rH 

rH 


* 

719.2 

17.8 


05 

id 
rH 
t- 


o 

-H 
O 
iH 


OJOHCO 
CO C5 CO d 
i-l C5 rH CO 

a i-i 

CM 


cm q 

id go 

CO 

10 

rH 


.3 

784.5 
50.8 


CO 

t- 

K0 
GO 


O 

c 

o 

T^ 



•a^uiioo 9I13H 'naoq 
AvajSt 'iTQAi. s.qSaaqnepj'BH "S 

•A^unao 81BH sua J^a-u 
'L ^poq; 'n9Ai ^U9uiuj3aoo 



GO O CO (M_ 

rH CO Oi OS 

<M CO CO GO 

CM lO 



lO GO t- p 

rH rH IM - rH 

rH t-I 
rH 



CO p 

i-i i-i 

GO 



•A^unoo ©ibh 'oaoqsti99.ro 

'lI9A\ S^JOAl J9}13A1 A^fO 

•a^uiiod 
9U99JO 'Ave^ng 'l[9Ai drana 



HffiHOC 
id rH CO i-i 



CO rH 
id O 



rH CO rH 

d CO CO- 
CO CI rH 
t- lO 



rH p CJ 

' CO CO 
iH iH 
rH 



GO CO CO 
rH id rH 



CM t- t- 

CO CO GO 



■A^iinoo 9U99jo 'AVE} 
-ng 'H9A\. s>uoa\ j9^ba\ a^iq 



CD p O O 

L~ O CO rH 

CO tH 



I- O 

ci id 



(N t- p 

r-i 05 GO 



■A^nnoo 9U99jf) 'Ave^ng; i 
s^trea 'o T 'll 8A 9rBpssi3.iQ ! 



CO CD CI 
' t^ tH 



OO 9U99J-Q 'AiB^ng 'S^Ugg 

•O T 'USA id"£§g spi 



'H9A\ '-Jf S9II0f UOSipBH 



"A^nnoo 9IBH 'q? r J0As.§p3AA. 
'II9AV s ( q^J0AvSp9A\. "H 'A\. 



■A^anoo 9I^h 



■jC^UriOD 3IBH 
'8 ipoi 'lI9A\. }lI9UIlIJ9AOO 



'OO nessTva '9niAU9if) Ji29u 

'I 'ON 'IIOA^ S,A\l.I9J "0 g 



•a^utiod n 9S | 
-siih 'oaoqs^ij 'ipay onqnj j 



go p co t- : 
d co id rH i 

OS (M ; 

! 


05 t- 

r-i O 
CM 
CM 


.9 
246.7 

7.2 


<M 1 
O I 


p 00 p CO I 
cd th ci ci 

lO i-l 

1 


lO rH 

cm' GO 

CO 


5.0 
121.2 

27.8 


IO 

id 

CD 

ci 


CO 

1-1 

CM 


p q CI p : 
t- rH ci T-i ! 

cq t-I ! 

1 


co io 
ci d 

iH 


1 rH rH CM 
! id GO t^ 

GO i-l 


iH 
d 
■M 


O 

o 

CM 


p CO O-l CI ' 

CO d CO rH ! 
O CO GO 

^ ! 


p O 
i-i i-i 

ci 


274.0 

323.4 

44.6 


cq 
1-i 

C35 
GO 


o 
o 

CM 


CO rH CI (M GO 

go i> id i> ci 

lO t-I 00 

o 

i-i 


1 iH 

!d 

so 


* 

865.1 
15.8 


p 
i-i 
GO 
CO 

co 


CO 
CD 

I-l 


q ci iq go | 
go co ; 


oq lq 

H CO 


175.9 
12.8 
19.4 


CM 

T-I 

rH 


rH 

CD 

1-1 



•A^ifeooq 



a 



«2ffi 



"^ 6 O cq 2 '3 5 

^2^ CD «« OM 



PkCQ 






o o 



O H? h a 

. u ^ cs r~J 






a 






O) 


> 


,Q 


K-l 


fcn 












03 




J3 




"oS 


> 


>;s 


~ 



§£ 



g OS HH 






363 

•A^unoo 3[Ba 
>[.ibzo 'siiao.tt. j9}bay A}io 


°3 ^ ^~ '" ' ' "* W 00 OS 05 1 
Ct CO t-» t- ! i-i CO 00 CI LO ! 

"* - - -f 

i-H 


256.3 
710 


X)iinoo 

OOJJOO '8SI.Kl.I3^Ua '[[9A\. UAVOJ, 


1 CI t-; <N 1 1 O O CI rt lO 1 

i- ' id | ai id o ci a> ! 

\ i-l CO | i-l rfi CO r-l ] 


175.!. 
398 


■Xiunoo AVBIJS 
-U8.I0 'Xa^u'B.ia 'H9M- uayoj, 


CO rH CO CO ' 1 OS t- iH lfl "O 1 

r-i ■* lo id I ! cii-io t^ id ! 

-* Hino) 
i-i 


:: cc 

_; & 

CI 


•A'^unoo AVBpoqo 
'sSuuids uionnQ '[[sav clggQ 


21.0 

4043.0 

35.3 

74.9 

3 8 
6098.9 

457.5 

9.9 


10744.3 

800 


■X^UIIOD 9ilJBI0 

'uos^oBf qpAV .inqding 


CICCpp 1 ! CO lO HH rH 00 * 
QOOOTti | ! ci co co t- I- 

OHO CO CO r-l 
O -r CI 
H 


2798.9 
110 


•OO 9>l.IBI0 'II9AV ;iBS PIO 


144.0 

11472.0 

122.4 

246. S 

18520.0 
* 

26.1 

8.2 


t- 1 

*+ ! 

LO 



CO ' 


Xiunoa BiqiuBosa 

'UO^EUlOia 'I19AV S.A9AI V '£> 


CO <N t- lO CO CO t CO ^ r-l CI 1 

in ci co oo co ci 1 ci os ■* id 1 

CO i-i ] 

1 


121.3 
377 


•Xiunoo 9[iq3W '9liqoj\[ 

JB3U 'l[9A\. S/00 110 u 0^00 


f-^iq^pr-i , . iq , co ci iiO; c, 
io id J— id - i i o i r-i os i Tji <=? 

l-ICO H 1 1 1 -f 1 00 r-l 1 1 r-l * 

r-l i 1 1 HH 1 CI 1 Ct 

r-l '• 1 rH 1 1 1 ' 1 


•A"^unoo 9lfqoj\[ 

'3&UIB0 'M 'H9A\ ;U9UIU.I9A0O 


i-i t-; -r i-i C- "S C HO 1 1 GO C» 

rti lo th co ! ; — i ci ci ai co ! co ~ 

CI C5 CI iO r-l OT 

rH iH 1 -V 


•a^uuod 
9 IIQ.°H 'IP^ l^Od BtUBqBlV 


* <n * cq i i i-j t- p r-j \a i 

o ci | i-i CO r-i ci CO ! 
CI r-l CI CO 

iH r-l rH 


401.2 
900 


1 

•A^unoo 9nqo]A[ '9J^BqBq 

UD^Ba 'H 9Ai - A\IO}OBJ guiUUBO 


(-; KO rH W I 1 00 O O O 1- 1 
CO -r r-i CO ! r-i ci ■*' 1- 00 ! 


247.7 
580 


•i}imoo .moq.iBa 
'BinBjng 'USA s.do.iqqnow 


iHCioqiq i i pt--cqooa) i 

CO CO ' CO ! r-i CO K5 Ci' LO ! 

CO r-l I- r-l 

rH r-l 


353.9 
350 


■A";unoo .moq.iBa 
'sijjbh 'H9AV s.doqsia 'H 


oo co th co i i coiqcococi i 
co lo id ci ! lo t-^ r-i rH oo ! 

CO rH CO rH rH 

1 1 <M 


388.4 
183 


•oo .moq.iBa 'uo^A"B[0 JB9U 
"II9AV s/oo doqsia-'i9nioo 


co oq co_ ci i i p iq co # t- rH i 

CO t^ r)i Hi | 1-; i- - t-J ci CO ! 

t- rH rH CI rH CI 

CI 


393.2 

277 


•A^unoo anoqjBa 'u^Aeio 
'I19av sJtJOAV aa^BAv. X;io 


p rfi os iq i i iq ci i- iq oo i 

rti ci ci ci ! co r-i lo id co ! 

O t-^ II CI O M 

rH 


372.1 
560 


A^unoo uo;Suiaoo 'bis 
-niBpuv 'I19A\ s ( oo HO uonoo 


i oq p ci lo i i p iq i> iq i 
! co i-i r-i ' ! ci t~ ci o ! 

|0 ! jrH t-Cl ! 


179.2 
1130 


a 

0) 
EC 

c 
o 

o 


Potassium (K) 

Sodium (Na) 

Magnesium (Mg) 

Calcium (Ca) 

Iron (Fe) 

Alumina (AI2O3) 

Iron oxide (Fe20s) and ali 

ina (AlsOs) 
Chlorine (CI) 
Sulphuric acid (SOi) 

Carbonic acid (HCO3) 

Silica (SiCM 

Hydrogen sulphide (H-S) 


"5 

OI 

«H 
O 

Q 



s & 



NDEX. 



Absorption of underground waters 34 

Add waters, chemical discussion, (Tablo V) 334 

Alakline waters, chemical discussion. (Tables I and II) 328 

Alkaline-saline waters, in chemical discussion. (Table III) 331 

Amount of water absorbed by porous rocks. 52; available to ar- 
tesian wells, 35. 
Analyses of Alabama Waters — 

Alabama Port well. Mobile 311 

Alabama White Sulphur Springs, Dekalb. 77 

Allen, Thomas B. well, Hale__I 159 

Allison Lumber Co. wells. Sumter 14.'> 

Altman. W. A. well, Sumter 133 

American Cotton Oil Co.. well. Mobile . 308 

Auxford, Y. T. wells, Tuscaloosa 121 

Awin and vicinity springs, Monroe 27C 

Bailey Springs, Lauderdale 103 

Bassetts Creek Sulphur Well at Jackson, Clarke 285 

Beavers. Dr. J. A. shallow well, Sumter 321 

Bishop, C. H. well, Barbour 243 

Bladon Springs, Choctaw 292 

Blount Springs and vicinity, Blount 78 

Borden-Wheeler springs, Cleburne 81 

Brantley town well, Crenshaw 202 

Bright, John W. shallow well. Mobile 306 

Brilliant Coal Mines well. Marion 96 

Bromberg Springs, Mobile 304 

Butler Springs. Butler 265 

Cahaba River water near Leeds, Jefferson 317 

Chambers Springs, Talladega 68 

Chandler's Springs. Talladega 67 

Cherokee Springs, Citronelle, Mobile 314 

Clayton city well, Barbour . 244 

Cold Springs, Blount 79 

Comer-Bishop Co. well. Barbour 242 

Cook Springs. St. Clair 89 

Cox. E. T. spring. Jefferson 87 

Crassdale plantation well, Greene 153 

Cullom Springs well, Choctaw 2!»7 

Demopolis city wells, Marengo 1X4 

DeSoto spring, Jefferson 90 

Dump well Eutaw, Greene : 153 

Elliott, J. A. & Son, Hale 160 

Enterprise well. Coffee 258 

Epes Cotton Oil Co. well. Sumter 140 

Evans Station well. Hale , 319 

Evans Station and vicinity wells. Hale 320 

Eutaw and vicinity wells, Greene 152 

Eutaw city well, Hale 153 



a — analysis given, r — record given. 



366 Index. 

Exchange hotel well, Montgomery 212 

Ferrill, C. C. well, Dallas 195 

Forinan, W. E. shallow well, Morgan 104 

Fort Gaines well, Mobile 312 

Gary Springs, Bibb 83 

Glenville and vicinity wells, Russell 237 

Glenwood springs, Blount 80 

Greensboro city wells, Hale 167 

Hale, Dr. R. H. shallow well, Sumter 134 

Hardenburgh. S. well, Hale 172 

Harrell, W. J. shallow well, Blount 80 

Hawkins well, Leeds mineral water, Jefferson 76 

Healing Springs, "Washington .._ 300 

Hightower, B. shallow well, Sumter 134 

Holt wells, TuscaloosaJ • 99 

Hosiery-mill well, Tuscaloosa 98 

Ingram well, Calhoun 82 

Ivey, G. A. well, Escambia 273 

Jones, Harden L. spring, Sumter 132 

Landers, A. M. shallow well, Calhoun 83 

Linden courthouse well, Marengo 188 

Little Egypt well, Greene 153 

Livingston and vicinity wells, Sumter 142 

Lock No. 8, well Black Warrior River, Hale 319 

Lock No. 7 well, Hale : 166 

McGraw, W. H. Caledonia shallow well, Wilcox 280 

McLendon, W. J. (Oswichee) well, Russell , 235 

Mentone Springs, Dekalb 91 

Mills, C. B. well, Sumter 133 

Mobile Cotton Oil Co. well, Mobile 308 

■ Moore, T. G. spring, Hale __ 319 

Moulthrop, brickyard well, Barbour 241 

Oyster Canning Co. well mouth of Bayou Labatre, Mobile 313 

Ozment spring, Tuscaloosa 116 

Ozark town well, Dale 25o 

Perry, Capt. E. C. well, Russell 238 

Pittsboro public well, Russell 237 

Prattville and vicinity wells, Autauga 216 

Ropers shallow well, Butler 265 

Salt well, Clarke 287 

Sanaqua Mineral Water, Madison 318 

Selma City "Waterworks well, Dallas 195 

Shelby Springs, Shelby 75 

Smith, John B. shallow well, Cherokee 83 

Southern Cotton Oil Co. well, Covington 260 

St. Clair Springs, St. Clair 74 

Stuarts Springs, Schuster, Wilcox 281 

Talladega Springs, Talladega 75 

Towne Spring, Jefferson__ 90 

Tidmore, J. C. wells, Perry 181 

Tunnel Sprins springs, Monroe 27 

Union Springs city waterworks well, Bullock 229 

University of Alabama, spring, Tuscaloosa 116 



a — analysis given, r — record given. 



Im.I'.x. 367 

Waller, Lichtman & Murphy Land & Development Co. well 

Hale 162 

Wedgworth, W. M. wells, Hale 164 

Williford's Landing well, Tuscaloosa 122 

Analyses of Alabama waters in Classified Tables 35] 

Annual precipitation map 30 

Temperature map 28 

Appalachian division, details of underground water in 66 

Geological characters 6 

Appalachian Valleys. Geological characters, 7; Details of un- 
derground waters in 71,317 

Artesian prospects 85 

Mineral waters 72 

Shallow waters 71 

Surface 1'eatnres 71 

Arrangement of strata in Alabama Coastal plain 61 

Artesian wells, defined, 51; general discussion concerning, 52; 
essential conditions of .52; modifying conditions, 57; de- 
cline or failure of, 62 ; .character of water of, 63: Judge 
Mobley's list of in Greene county, 146. 
Artesian wells, shallow wells, and springs, referred to in this 
report. List of. 

Abraham Church well. Montgomery 214 

Adams, Mrs. well, Pickens ! 130 

Adams, D. well, Macon 222 

Adams, James well. Macon 222 

Adams, R. B. well. r. Russell 236 

Agnew, Peyton well. Hale 170 

Akron & Vicinity wells. Hale 161 

Alabama City well, Etowah --. 93 

Alabama Portland Cement Co. well, Demopolis, Marengo 185 

Alabama Polytechnic Institute well, Auburn, r. Lee 223 

Alabama Port well. a. Mobile 311 

Alabama White Sulphur Springs, a. Dekalb 76 

Alexander, Alex, well, Greene 156 

Alexander City wells, Tallapoosa 70 

Alexander, J. S. wells, Perry 178 

Alexander, W. B. wells, Perry 178 

Aliceville & Vicinity wells, Pickens 125 

Allen, B. M. well. Hale 175 

Allen, Mrs. Charles well, Marengo 186 

Allen, R. P. well. r. Marengo 185 

Allen. Thomas B. well, a. Hale 159 

Allison Lumber Co. wells, a. r. Sumter 142 

Alston, S. F. well, r. Tuscaloosa 118 

Altaian, W. A. well, a. Sumter 133 

American Cotton Oil Co.'s well, a. Mobile 308 

Andalusia & Vicinity wells, Covington , 259 

Andalusia Town well, r. Covington 259 

Anniston wells, Calhoun 85 

Anthony, M. well, r. Autauga 217 

Ardt, Frank well, Cullman 95 

Arnold, A. & Co. well, Cullman 95 

Atlantic Compress Co. well, Bullock 229 



a — analysis given, r — record given. 



368 Index. 

Auburn well, Lee 71,223 

Autaugaville well, Autauga 219 

Auxford, Y. T. wells, a. r. Tuscaloosa '. 121 

Awiu springs, Wilcox 281 

Awin & Vicinity springs, a. Monroe 276 

Bailey springs, a. Lauderdale 103 

Baker, T. A. well, Pickens 130 

Baker, J. M. well, Dallas '. 196 

Ball, Henry well, Pickens : 127 

Baldwin, Martin well, Montgomery 213 

Baltzell, W. B. well, Greene 157 

Bark, J. well, Russell 229 

Bark, W. H. well, Russell 233 

Barackias well, Montgomery 211 

Barnes, Wiley well, Sumter 136 

Barnett, A. V. well. Bullock 227 

Barren Fork spring, Madison : 102 

Barrett's well. Mobile , 313 

Bassetts Creek Sulphur well, at Jackson, a. Clarke 285 

Battles, Gus well, Russell 236 

Bean place well, Dallas 202 

Beavers, Dr. J. A. shallow well, a. Sumter 320 

Bell, Elijah place well, Dallas 200 

Bell, Turner wells, Dallas 200 

Bell, Mrs. J. W. well, Sumter 135 

Bell place well, Sumter 136 

Bennett, R. L. wells, Hale 171 

Bently Lumber Co. well, r. Crenshaw : 262 

Bessie Minge Mfg. Co. well, Marengo 185 

Billingsley place wells. Perry 180 

Bishop, C. H. well, a. r. Barbour 242 

Blackman, J. S. well, Perry 181 

Blackman, Cobb well, r. Greene 157 

Bladon Springs, a. Choctaw, 291 

Blacksher, J. M. (at Maros) well r. Monroe 279 

Blacksher Lumber Co. wells, Mobile 309 

Black Warrior Lumber Co. well, Marengo 185 

Blair, Dr, spring, Jackson 92 

Bledsoe, E. P. well, Macon 223 

"Bleak House" place wells, Hale 174 

Blevin, Wm. well, Cullman 95 

Blount Springs & Vicinity, a. Blount 77 

Blount & Ward well, r. Hale 167 

Bolen well, r. Clarke 287 

Boligee & Vicinity wells, Greene 156 

Bonner Place well (Mr. Hagaman owner), Pickens 126 

Borden-Wheeler springs, a. Cleburne 80 

Borden, Cheney well, Hale 168 

Bouchelle, E. F. well, Greene 156 

Bouchelle, H. T. well, Greene 156 

Boynton, M. A. well, Wilcox 282 

Bradford well, (Abe Gray owner), Pickens 126 

Brassfleld, D. S. well, Greene 157 



a — analysis given, r — record given. 



[ndex. 369 

Brannon, J. S. well, Russell l'.".I 

Brantley Town well, a. Crenshaw 262 

Brantley & Vicinity wells, Crenshaw . 262 

Brewton & Vicinity wells, Escambia 269 

Bright, John W. shallow well, a. Mobile 306 

Brillianl Coal Mines well, a. Marion 96 

Britton, 1>. II. well, Marengo L85 

Brockton well, Coffee 257 

Brockway, C. J. well, Sumter 136 

Bromberg Springs, a. Mobile , 304 

Brown, W. A. well, Jefferson 97 

Brown, Louis well. Sumter 141 

Brown well, Perry 182 

Brown, J. C. well. r. Marengo 186 

Brown Station wells. Dallas 200 

Buckeye Cotton Oil Mill well. r. Dallas 197 

Bughall well, Bullock 228 

Bullock well, Greene 157 

Burns. J. C. well. r. Autauga 217 

Burton Hill wells. Greene 157 

Burrough's Springs, Perry 177 

Bush well. Clarke 288 

Butler Springs, a. Butler 205 

Butler well, Choctaw 297 

Butler & Vicinity springs. Choctaw 294 

Cahaba "Great Well," r. Dallas 193 

Cahaba River water near Leeds, a. Jefferson 317 

Cahaba wells. Dallas 192 

Caldwell, J. W. gin well. r. Russell 237 

Capps Creek spring. Lawrence 104 

Caraway place well, Pickens 126 

Carlisle well. Etowah 94 

Carmichael place well, Dallas 204 

Carrington, J. B. well. Walker 94 

Carson. W. N. wells, Dallas 204 

Carter, J. II. well, Cullman 95 

Cates well, r. Marengo 190 

Catherine & Vicinity, Wilcox 282 

Cawthon Cotton Mills well, Dallas 194 

Cedar Creek Mill Co. well, r. Escambia 271 

Cedarville & Vicinity wells. Hale 169 

Central Coal & Iron Co. wells, Tuscaloosa 98, 99 

Chambers Springs, a. Talladega 03 

Chandlers Springs, a. Talladega 67 

Chambers place well, Dallas 203 

Chapin Montgomery waterworks well. Montgomery 209 

Chapman Springs. Choctaw 293 

Chapman wells, Butler 267 

Chapman, L. L. well. Autauga 216 

Cherokee Spring, Citronelle, a. Mobile 304 

Cherry place well, Pickens 128 

Chesson, A. B. well. Macon 222 

Chesson well. Macon 222 

Chisholm, Mrs. well. Perry 182 



a — analysis given, r — record given. 



370 Index. 

Chisholm, Gordon well, Perry , 182 

Chisholm, Johnny r, Perry : 182 

Cliocco Springs, Talladega : 81 

Citronelle well, Mobile 314 

Clarke place well, Greene 154 

Clarke place well, Dallas 200 

Clark, A. H. well, Montgomery 214 

Clayton City well, r. a. Barbour 244 

Clinton Springs, Perry : 177 

Clinton & Vicinity wells, Greene 152 

Cochrane, W. A. well, Dallas —. 203 

Cochrane, John wells, r. Pickens 125 

Coden Station well, Mobile 313 

Cold Springs, a. Blount 79 

Cole place well, Greene 157 

Coleman, Judge wells, Hale . 162 

Coleman, Judge T. W. well, Greene ■ 155 

Collins, Mrs. Julian well, Hale 175 

Collins, C. W. wells, Hale 175 

Columbia well, Houston 253 

Comer-Bishop Co. well, Russell 237 

Comer-Bishop Co. well. r. Barbour 242, 243 

Comer, B. B. well, r. Barbour 242,243 

Cook Springs, a. St. Clair 89 

Cook Montgomery well, r. Montgomery 210 

Cook, Dr. T. H. G. well, Pickens 129 

Cooper, L. C. well, Russell 1 234 

Cooper, L. C. wells, Crenshaw 262 

Cotton Oil Co. well, r. Hale 167 

Cooper place well, Perry . 179 

Cox, E. T. spring, a. Jefferson 87 

Cox, Jesse well, r. Montgomery 1 213 

Carroll, Mrs. well, Dallas 198 

Crabtree, O. V. well, r. Hale 162 

Creek place well, Dallas 206 

Craig, Edward well. Perry 178 

Crawford. J. P., r. Russell 233 

Crenshaw place well, Dallas 202 

Crassdale plantation well, a. Greene 153 

Crenshaw place well, Greene 155 

Creswell, S. L. well, Greene 155 

Groom, Mrs. Mattie place well, Hale 171 

Cullman wells, Cullman -. — 95 

Cullman City well. Cullman 95 

.Cullman Co. Oil Cos. well, Cullman 95 

Cullom Springs well, a. r. Choctaw 295 

Cummings, C. D. wells, r. Hale 160, 163 

Curtis well, Morgan 106 

Cypress switch well, Hale 160 

Davidson, A. C. well, Dallas 200 

Davis place well, Perry 179 

Dayton wells, Marengo 186 

Deasons, W. S. well, Bullock 229 

Dedman place wells, Dallas 205 



a — analysis given, r — record given. 



Index. 371 

Degraffenreid, E. W., Hale nil 

DeLacy, J. M. well, Russell 234 

Demopolis & Vicinity wells, Marengo 183 

Demopolis City wells, r. a. Marengo i 183 

Demopolis Cooperage Co. wells, Marengo is:; 

Demopolis Ice & Cold Storage Co., Marengo "_ 184 

Deprez, L. W. well, Franklin 107 

DeSoto spring, a. Jefferson 00 

Dollarhide Co. well, Greene 155 

Dothan Ice Co. well, r. Houston 253 

Dotlian Town well, r. Houston 253 

Dothan City Water Co. well, Houston 253 

Downey, Dr. W. T. spring, Perry 170 

Downing, Wiley well, r. Escambia 271 

Downing, E. well, Escambia 271 

Downs and Vicinity wells, Macon 222 

Drake place wells. Hale 175 

Dreher, A. & Co. well, Cullman 95 

Duke place well, Dallas 205 

Dump well, Eutaw, a. Greene '. 153 

Dunham Lumber Co. well, Butler 207 

Dunlap, C. C. well, Greene 156 

Dunlap place well, Hale 175 

Durands Bend well, Dallas 198 

Edgar well, r. Clarke 288 

Edwards, Adam place well, Dallas 205 

Edwards, George well, Bullock 228 

Edwards, Gus well, Bullock 227 

Edwards, Snyder well, Dallas 205 

Egypt place wells, Hale 170 

Elba & Vicinity wells. Coffee 257 

Eleanor town well, Dallas 203 

Elkdale Park well, r. Dallas 197 

Elliott, J. A. & Son, r. a. Hale 159 

Ellis & Dunaway well, Dallas 199 

Enterprise well. a. Coffee 258 

Epes Cotton Oil Co. well, a. r. Sumter 139 

Epes & Vicinity wells. Sumter 1":' 

Erie Landing well, r. Hale 16(5 

Erie & Vicinity wells, Greene 157 

Erwin, Geo. wells. Hale , 170 

Evans Station well. a. Hale 319 

Evans, B. S. well, r. Hale 102 

Evans Station & Vicinity wells, a. Hale 162-320 

Evergreen Town well, Conecuh 208 

Eufaula Oil & Gas Co. well, r. Barbour 240 

Eut'aula & Vicinity wells. Barbour 240 

Eufaula Water Co. well, Barbour 240 

Bulow well, Dallas 202 

Eutaw & Vicinity wells, a. Greene 152 

Eutaw City well, a. Greene 153 

Eutaw Courthouse well. r. Greene 153 

Exchange Hotel well. a. Montgomery 212 

Farmers Gin & Warehouse Co. well. Hale 172 



a — analysis given, r — record given. 



372 Index. 

Faunsdale & Vicinity wells. Hale 175 

Faunsdaje & Vicinity wells, Marengo 185 

Faunsdale Oil Mill well, Marengo 186 

Fayette well, Fayette '. 114 

Felix & Vicinity wells. Perry 1 170 

Ferguson Place well, Pickens 128 

Ferrill, C. C. well, a. Dallas 195 

Findlay, John well, r. Hale 160 

Findlay, W. A. well, Escambia , 272 

Fisher, W. M. well, Autauga 217 

Fitzgerald, J. T. wells, Perry 181 

Fitzpatrick well, Bullock 227 

Flatwoods or Post Oak wells, Marengo 188 

Flower. W. M. well, Butler 266 

Flower, W. J. Lumber Co. wells, Butler 266 

Ford. C. W. spring. Perry 177 

Forkland & Vicinity wells, Greene 157 

Forman, W. E. well, a. Morgan 104 

Fort, Mrs. E. W. well, Dallas 201 

Fort, Mrs. L. G. well. Dallas 202 

Fort Gaines well, r. a. Mobile 312 

Fort Davis, wells at, Macon 223 

Foster, J. Manly wells, r. Tuscaloosa 119 

Foster, Guy well, Tuscaloosa 120 

Foster, R. M. place well. Perry 176 

Franklin Springs, Franklin 102 

Friedman & Loveman well, r. Tuscaloosa 119 

Friedman, B. deep boring, Tuscaloosa 97 

Furniss, Dr. J. P. well, Dallas 200 

Gainesville Mill well, Sumter '. 137 

Gainesville & Vicinity wells, Sumter 137 

Gaineswood well, Marengo 185 

Gallion & Vicinity wells, Marengo 185 

Gallion & Vicinity wells. Hale 174 

Galloway. Dr. J. M. well. Montgomery 214 

Garber Bros, well, Hale 174 

Gardner & Somerville well, Pickens 126 

Gardner place well, Pickens 126 

Gary Spring's, a. Bibb 82, 83 

Gate City wells, Jefferson 86 

Geneva Public well, r. Geneva 254 

Geneva Town well. r. Geneva 255 

Gentry, J. W. well, Sumter 135 

Gewin, A. B. well. Perry 180 

Gewin. A. B. well, Hale 170 

Gholson Place well, Marengo I 186 

Gholson, Bob well, Bullock 227 

Gibson place well, Pickens 126 

Gill, Andrew well. Dallas 198 

Gill place well, Dallas 203 

Gilman, E. well, r. Dallas 196 

Gilmer, W. J. & E. T., Perry 182 

Girard well, r. Lee 224 



a — analysis given, r — record given. 



Index. 373 

Glenville & Vicinity wells, a. Russell 23-7 

Glenwood spring, Blount SO 

Gold Dusl Farm well, Pickens 12N 

Goldsby place well, Pickens 12 ( .» 

({oyer wells. Lawrence 107 

Graham well, mouth of Bayou Coden, Mobile 313 

Graham, J. C. well, Bullock 229 

Graham, Malcolm well, Autauga 217 

Greenville City well, Butler 266 

Groves, F. M. well, Sumter 136 

Grandview well, Elmore 221 

Gray. Eli well. Bullock 227 

Greensboro & Vicinity wells. Hale 167 

Greensboro City wells, a. Hale '167 

Oriel Bros, well, Montgomery 214 

Griffin. R. L. well. Hale 160 

Haddock, F. P. well, Russell 234 

Hairston well, Greene 156 

Hairston, T. J. well, Lowndes 207 

Hale. Dr. R. H. shallow well, a. Sumter 153 

Hale Spring, Jefferson 90 

Hall. J. W. place well, Greene 155 

Hamburg Station & Vicinity wells. Perry 181 

Hammack, P. Ii. well. r. Montgomery 214 

Hardaway wells. Macon 222 

Hardaway Town well, Macon _, 1 222 

Hardenburgh, S. well. a. Hale 172 

Hardin, G. H. well, r. Russell 235 

Harmon, T. B. well, Pike 224 

Harralson. H. A. well, Dallas 196 

Harrel. Tom place well, Dallas 202 

Harrell, W. J. well, a. Blount 80 

Harrel place well, Dallas 201 

Herrington & Vicinity wells, Escambia 271 

Harris, Will well, Macon 222 

Harris, E. M. well. Franklin 107 

Harris, Aaron well, Pickens 126 

Harris, J. G. well, Greene 154 

Harris, W. S. well. Macon 222 

Harris & Vicinity wells, Barbour 242 

Hartford Town well, Geneva 255 

Hartsell well, Morgan 107 

Hatch, Bill well, Dallas _' _- 205 

Hatchechubbee & Vicinity wells, Russell 234 

Hatcher plantation wells, Russell 236.238 

Hatcher. Dr. well. Greene 156 

Hawkins well, Leeds mineral water, a. Jefferson 75 

Haynesworth Springs, Perry 17<i 

Hayneville well, Lowndes 208 

Hazel Green well, Madison 105 

Healing Springs, a. Washington 299 

Henderson Lumber Co. well. r. Covington 261 

Heard, G. T. wells. Pickens 126 



a — analysis given, r — record given. 



374 Index. 

Hermitage place well, Hale 174 

Heron, M. S. wells. Hale 171 

Hestell Cotton Mill well, Dallas 196 

Hightower B. shallow well, a. Sumter 134 

Hillman, Emma R. well, Greene 157 

Hilton, Dr. well, Pickens 125 

Hogue, J. J. well, Hale 172 

Holt wells, a. Tuscaloosa 97, 99 

Hood, Mrs. E. G. well, Pickens 127 

Hornbuckle place well, Perry 177 

Horse-Shoe Lumber Co. well, Covington 261 

Horton, Mose place well, Greene 152 

Hosiery-Mill well, a. Tuscaloosa 98 

Huggins, Dr. J. well, Hale 172 

Hunter place well, Dallas 198 

Hunter, Mrs. F. lu. well, Dallas 200 

Hurt, Josh place well, Dallas 203 

Hurtsboro Public well, Russell 233 

Hurtsboro & Vicinity wells, Russell 233 

Ice-factory well, Butler 266 

Inge, W. B. well, Hale 161 

Ingram well, a. Calhoun 82 

Ingram, C. E. well, r. Russell ^ 234 

Irvin plantation well, Hale 171 

Ivey, G. A. well, a. Escambia 273 

Jackson place well, Pike 224 

Jackson Mineral Springs, Choctaw 294 

Jackson sulphur well, Clarke 285 

Jernigan, J. A. well, Escambia 271 

Jernigan, J. L., Escambia 272 

John, S. W. place well, Dallas 201 

Johnson well, (oprings), Madison 102 

Johnson, G. B. well, Perry 180 

Johnson place well, Dallas 1 203 

Johnson, Strong place well, Dallas 204 

Jones, Amos well, Montgomery 214 

Jones, C. O. well, Dallas 201 

Jones & Stewart well, Perry 181 

Jones, Mrs. L. R. well, Dallas 198 

Jones Estate well, Dallas ; . 201 

Jones, Henry A. wells, Tuscaloosa 119, 120 

Jones, Dr: B. T. well, r. Pickens 129 

Jones, Winston well, Pickens 129 

Jones, Harden L. spring, a. Sumter 132 

Jones, Sam T. wells, r. Sumter 139 

Jones, W. A. C. well, r. Sumter 140 

Jones place well, Greene 156 

Jones, Madison Jr. wells, a. r. Hale 165 

Jones, A. C. well, Hale 169 

Jones Springs, St. Clair '. 73 

Kaiser, Dr. Spring, Winston 92 

Kaolin Station well, Russell 232 



a — analysis given, r — record given. 



Im'K.x. 375 

Karnegie, Mrs. C. L. well, Hale 171 

Karnegie place well, Hale 171 

Kay, Moses well, Greene L56 

Keego well, Escambia 271 

Kellennan deep boring, Tuscaloosa 07 

Kelly Bros, wells. Hale 169, 170 

Kendrick Bros, wells, Dallas 200 

Kendrick, W. II. wells, Dallas 201 

Kimbrough, E. L. wells, r. Hale 104. 166 

King place well. Dallas 204 

King, Mrs. wells, Dallas 201 

King, Henry well, Tuscaloosa 121 

King place well, Pickens 130 

King, W. D. well. Pickens 130 

Kirksey place well, Wilcox 282 

Kli. Geo. A. well, Marengo 184 

Knight, L. A. well, Sumter 138 

Knight place wells, Hale 170 

Knox, R. P. well, Marengd 185 

Knox Academy well, Dallas 190 

Kyle. T. S. shallow well. Etowah 94 

Lamb, L. C. wells, r. Russell 230 

Landers, W. H. well, r. Hale 172 

Landers. A. M. shallow well, a. Calhoun 82 

Landlord, Mrs. L. A.. Sumter 138 

Laneville & Vicinity wells. Hale 174 

Langford's spring. Lauderdale 103 

Lanett wells, Chambers 70 

Latimer, E. S. well, Greene 157 

Lawson, W. H. well, r. Montgomery 214 

Lawson, Booker wells, Pike 225 

Lay springs, Dekalb 91 

Leder Oil Co. well, Marengo 184 

Lee's spring, Lauderdale : 103 

Lee Place well, fickens 127 

LeGrand, Paul well, r. Montgomery 213 

Lewis. Mrs. C. A. well, Greene 157 

Lewis. I. F. well. Hale 174 

L. & N. R. R. wells, Dallas 199 

Ligon Springs, Colbert 101 

Linden Courthouse well, a. Marengo 188 

Lindsey, Martin, Hotel well, Escambia 272 

Lindsey, M. well. Escambia' 272 

Linwood wells, Pike 225 

Little Egypt well, a. Greene 153 

Little. J. J. wells. Sumter 136 

Livingston & Vicinity wells, a. Svimter '_ 141 

Lock No. 8, Black Warrior River well. a. Hale 319 

Lock No. 9 wells, r. Hale 160 

Lock No. 8 well. Hale 161 

Lock No. 7 well r. a. Hale 165 

Lock No. 5 well, r. 169 

Logton wells. Pike 225 



a — analysis given, r — record given. 



376 Index 

London, Mr. well, Hale 175 

Long, R. C. well, Pickens 129 

Long, N. W. E. well, Russell 236 

Long, R. H. well, Sumter 137 

Long & Patterson wells, Sumter 138 

Long, R. H. well, r. Sumter 139 

"Long Farm" place wells, Hale 171 

Lovelace well, Perry : " 177 

Lower Salt works Sulphur Spring, Clarke 283 

Lubbub Creek well, Pickens 125 

Lyon, Andrew well, Sumter 136 

Madden place, well. Hale 175 

Magnesia spring, Perry 177 

Manning, Mat well, Escambia 272 

Manning place well, Pickens 128 

Margaret S. T. well, Russell .. 236 

Marion & Vicinity wells, Perry 178, 180 

Marion Junction wells, Dallas 202 

Marion Town well, Perry : 178 

Marion Junction & Vicinity wells, Perry 182 

Marks, Deb. well, r. Greene . 157 

Marsh place well, Sumter 138 

Martin, N. N. well, Escambia 272 

Martin's Station <x Vicinity wells, Dallas 199 

Martin, A. J. well, Dallas 199 

Martin, E. B. well. Dallas 199 

Martin, W. H. well, r. Hale 161 

May, Miss K. C. well, Hale 164 

Mauldin place wells, Hale 171 

May, Mrs. Ben well, Sumter 138 

Mayhew, Mrs. M. E. Pickens 125 

Mayhew place well, owned by E. Stuart, Pickens 126 

Mayor, W. T. well, Escambia : 272 

McCaa, Mrs. E. A. well, Pickens 126 

McCaa, Billy well, Pickens 126 

McCaa place well, Pickens 126 

McCarroll, Mrs. well, Perry 181 

x.-i.cCreary place well, Dallas . 203 

McClure Lumber Co. well, Greene 154 

McCurdy, W. D. well, r. Lowndes 207 

McDonald, T. L. well, Russell 236 

McDonald, J. H. well, Pickens ^ 130 

McGill, well, Dallas 196 

McGraw, W. H. (Caledonia) shallow well, a. Wilcox 280 

McKinstry, L. E., Pickens 1 126 

McKiustry, Mrs. L. E. well, Pickens 126 

McLendon, W. J. (Oswichee) well a. Russell 234 

McMicken well, r. Russell 234 

Mentone springs, a. Dekalo 91 

Middle place well, Dallas 206 

Mills, C. B. shallow well, a. Sumter ' 133 

Millions, J. F. well, Dallas 199 

Milhous, Phil well, Dallas 199 



a — analysis given, r — record given. 



Index. 377 

Millions. P. Walter wells. Dallas 203 

Millwood & Vicinity wells. Hale 168 

Mingo. John well. r. Marengo 185 

Minneice, Tom well. r. Sumter 139 

Mitchell Station wells. Bullock -_!27 

Mitchell well. Dallas 201 

Mize, .1. < '. well. Tuscaloosa 117 

Mobile Oil Co. well. r. Mobile 309 

Mobile Electric Light Co., Mobile 308 

Mobile Brewery Co. well. r. Mobile 307 

Mobile Cotton Oil Co. well. a. Mobile 308 

Mobile & Vicinity wells. Mobile .-KIT 

Mohr, Paul well. Cullman 95 

Molette place well. Dallas 20(5 

Monette, Jack wells, Hale 1GG 

Montgomery wells. Montgomery . 209 

Montgomery City Waterworks well. r. Montgomery 212 

Montgomery Brewery Co. wells, Montgomery 212 

Moore, T. G. spring, a. Hale 319 

Moore. D. L. wells. Hale 17.°. 

Moore. Will wells. Dallas 202 

Moore place well. Dallas 203 

Moore, Wm. piace, well, Dallas 204 

.Moore. John well. Dallas 205 

Moore. Andrew J. wells. Hale 173 

Moore. T. well. Sumter 130 

Moore spring. Limestone 102 

Mooring, Mrs. well, Sumter 138 

Morgan, Senator John T. well. Sumter 139 

Morris Lumber Co. well, Greene 255 

Morrisette, F. S. well. Hale 171 

Morrisette, F. S. plantation well. Hale 172 

Morrison, W. M. well. r. laissell 235 

Moseley, Dr. E. B. wells, Dallas 204- 

Moss Grove place wells, r. Dallas 204 

Meulton Valley wells. Lawrence 107 

Moulthrop Brickyard well, r. a. Barbour 241 

Moundville & Vicinity wells. Hale 159 

Murphy. Will well. Tuscaloosa 119 

Murphy. W. H. wells, r. Hale 109 

Nelson, W. P. well. Hale 173 

Nelson place well, Dallas 200 

Nelson, L. Q. well, Autauga 218 

Newberne & Vicinity wells. Hale 171 

Newberne well. Hale 173 

New Market well. r. Madison 102. 105 

Nolen place well, Pickens 126 

Norman spring, Perry 176 

North of Chunnennugga Ridge wells, Bullock 227 

Near Line of So. R. R. wells. Dallas 200 

Oak Grove place well. Pike 224 

Oakman well. Walker 1 94 



a — analysis given, r — record given. 



378 Index. 

"Oak Grove Place" wells, Hale 174 

Ogden well, Lamar , 114 

Old Bridgeville well, Pickens 125 

Old Hamburg wells, Perry ITS 

Old Spring Hill well, Marengo. 186 

Old Salt wells, Washington 300 

Old Salt wells, Clarke 284 

Oliver, Will well, Sumter 130 

Oliver, Robert well, Sumter 136 

Oliver & Oliver well, Sumter 136 

Orion & Vicinity wells, Pike 224 

Orrville town well, Dallas ' 199 

Orrville & Vicinity wells, r. Dallas 199 

Otts, Lee well, r. Hale 167 

Otts, J. M. P. well, r. Hale 167 

Overstreet place well, Dallas 202 

Overstreet, E. M. well, Dallas 204 

Oyster Canning Co.'s well, a. (mouth of Bayou Labatre), 

Mobile _ 313 

Ozment spring, a. Tuscaloosa '. 116 

Ozark town wells, a. Dale 256 

Palmetto place well, Marengo 186 

Parker, wells Montgomery, r. Montgomery 211 

Parker, Geo. H., Cullman 95 

Portersville Bay Shore wells, r. Mobile 313 

Patterson, J. W. well, r. Sumter 137 

Patton, A. P. well, Greene 152 

Patton, Jeff well, Greene 152 

Peck place well, Hale 170 

Peebles, W. B. well, Pickens 128 

Peebles, Wm. well, Sumter 136 

Pegues well, Dallas 201 

Penned wells, Dallas 202 

Peoples Oil Mill well, Dallas : 196 

Perry, Capt. E. C. well, r. a. Russell 238 

Perry, Jim well, r. Russell 234 

Perry, Mrs. well, Greene . 156 

Persons Crossing well wells, Russell 236 

Perrin, Dr. well, Greene 156 

Peterson, W. A. well, Pickens 127 

Pettusville spring, Limestone 101 

Pickens, Ned well, Hale 173 

Pickens place well, Hale 169 

Pickensville & Vicinity wells, Pickens 127 

Pierce, W. E. well. Montgomery 214 

Pine Hill well, Wilcox 282 

Pinson, J. H. well, Sumter 137 

Pitts, F. P. well, r. Russell 237 

Pittsboro public well, r. a. Russell 236 

Pittsboro & Vicinity wells, Russell 236 

Pharr, J. R. place well, Wilcox ' 282 

Phifer, W. P. well, Hale 160 

Pollard wells, Escambia 271 



a — analysis given, r — record given. 



Index. 379 

Poplar spring, Perry lie. 

Pratt, Mrs. Julia A. well, r. Autauga 217 

Pratt City wells. Jefferson 9(1 

Pratt, Daniel wells. Autauga 217 

Prattville & Vicinity wells, r. a. Autauga 215, 216, 217. 218, 210 

Prattville Junction well, r. Elmore 220 

Pringle, P>. F. well. Escambia 272 

Pushmataha spring, Choctaw 294 

Quarles, well r. Tuscaloosa 120 

Radfordville wells, Terry 178 

Rainer. S. P. well. Bullock 22S 

Rainer. J. H., Bullock 228 

Rainey, Mrs. well, Dallas 205 

Ralston well. Mobile __2 313 

Rascoe well. Dallas 201 

Rice, .Dr. Clarence well, Autauga 217 

Richardson place well. Pickens 128 

Rklgeway, Andrew well, Dallas 205 

River Falls & Sanford wells, Covington 2(10 

Reese place well. Dallas 205 

Ringos Bluff well, Pickens 126 

Roba well, Macon 223 

Roberts, Judge T. W. well. r. Greene 154, 155 

Roberts well, r. Escambia 273 

Robertson, J. X. well, Tuscaloosa 117 

Rogers, N. a. wells, Sumter 135 

Rogers, J. P. wells, Sumter 136 

Rogers. Mac. well, Sumter 136 

Rogers. John well, Sumter 137 

Rogers, John A. well. r. Sumter 138 

Rogers, Sallie, r. Sumter 138 

Rogers, J. A. well. Sumter 139 

Rogers, W. R. wells, r. Pickens 127 

Ropers well, (shallow), a. Butler 263 

Roscoe place well, Dallas . 204 

Rosenau Bros, well, Tuscaloosa 97 

Ross place well, Marengo 185 

Ruffin, Tom well, Hale 169 

Rugh place well. Hale 174 

Russell, Hart well, Macon 223 

Rutherford & Vicinity wells, Russell 235 

Rutherford, H. M. well, r. Russell 235 

Rutland, Frank well. Bullock 227 

Salt well near Bolen well, a. Clarke 2S7 

Salt Works well, r. Clarke 288 

Sample, W. M. wells, r. Hale 163 

Sanaqua Mineral Water, a. Madison 317 

Sanders Mill well, Hale 170 

Sanders place well, Dallas 198 

Sawyerville & Vicinity wells. Hale 166 

Scarlock springs, Choctaw 294 



a — analysis given, r — record given. 



380 Indkx. 

Schuler, E. T. well, Etowah + 94 

Schweizer, J. ij. well, Dallas 196 

Scott Hill well, Lowndes 207 

Scott, Howze well. Perry 180 

Scotts Station wells, Perry 180 

Seay, Governor well, Hale : 164 

Seale Court House well, Russell 234 

Seale & Vicinity wells, Russell 234 

Searight wells (So. Cotton Oil Co.), Crenshaw 263 

Selden Place well, Marengo 186 

Seldon, E. C. place well, Greene 156 

Selnia Race Track well, Dallas 196 

Selma & Vicinity wells, Dallas 194 

Selina City Waterworks well, r. a. Dallas 194 

Selma Council Chamber well, Dallas 195 

Shelby Springs, a. Shelby ' 75 

Shoal Creek Lumber Co. well, r. Monroe 278 

Shopton & Vicinity wells, Bullock 227 

Silver place wells, Pike 224 

Simon Tract place well, Hale ,j. 175 

Singleton & Linton well, r. Bullock 228 

Singleton, A. E. well, Bullock 228 

Sipsey Mill well, Pickens 125 

Sipsey River wells, Pickens 125 

Sipsey well, Greene 152 

Sledge & Leonard well, Hale 170 

Smaw place well, Marengo : 186 

Smith, Craig well, Dallas 199 

Smith, C. M., well, r. Lowndes 207 

Smith. Ebo well, Dallas 205 

Smith, E. I. well, Autauga 216 

Smith, John B. shallow well, a. Cherokee 83 

Smith, Judge A. P. well, r. Greene 152 

Smith, Major M. M. well, Autauga 219 

Smith, T. L. well. Sumter 139 

Smith, Walter well, Perry 179 

Smith, W. T. Lumber Co. well, Butler 267 

Smith. Wash well, Dallas 205 

Somerville, J. B. well, Pickens 129 

Southern Cotton Oil Co. well, a. Covington 260 

Southern Cotton Oil Co. well, Crenshaw 262 

Southern Cotton Oil Co. well, Butler 266 

Spangenburg Iron spring. Choctaw __ 294 

Spigener, G. Cook well, Autauga 217 

Sprague Junction wells, Montgomery 214 

Spring Hill well, Barbour 244 

Sprott wells, r: Perry 177 

St. Bernard College well, Cullman 95 

St. Clair springs, a. St. Clair 73 

State Farm wells, Elmore 221 

Stewart's well, Lauderdale 102 

Stewart, J. E. well, Pickens 127 

Stewart's & Vicinity wells, Hale 160 

Stuart Springs, Schuster, a. Wilcox 281 



a — analysis given, r — record given. 



Index. 381 

Stevenson place well, Dallas , 205 

Stollenwerck, G. 1>. well, Terry . pso 

Stone Station well, Montgomery 214 

Stone well, Lamar 114 

Stone, II. L. well, Pickens 127 

Stone Public well, Pickens 129 

Stone. Nan well. Sumter 13G 

Stovall's wells. Walker 95 

St. Stephens well. Washington 301 

Stubh. I. K. well. Escambia 272 

Stubbs, Henry well, Dallas 202 

Sulligent wells. Lamar , 114 

Snmmerfield Oil Mills well, Dallas IPS 

Sumter Lumber Cos. well. Sumter 143 

Snmterville & Vicinity wells, Sumter 141 

Sunshine well. Hale -2 174 

Suttle & Jones plantation wells. Perry 179 

Swift place wells. Perry 179 

Swilley place well, r. Greene 155 

Talladega springs, a. Talladega 74 

Tallahatta springs. Clarke , 283 

Talman, R. P. well. r. Russell 23.1 

Tart. Mrs. A. M. well. Sumter ' 140 

Taylor place well, Sumter 137 

Taylor, Dave well. Dallas 202 

Thigpen, W. A. well, Perry ISO 

Thompson Station well, Bullock 227 

Thornton place well, Greene 156 

Thornton springs, Choctaw 290 

Tidmore, J. C. wells, r. a. Perry 180 

Tinker, Harris place wells. Hale 171 

Todd's springs, Lauderdale 103 

Tompkins, Judge H. B. well, Colbert 107 

Town Creek, tar spring. Lawrence 104 

Towne spring, a. Jefferson 90 

Troy City well, r. Pike 225 

Troy Oil & Chem. Co. well. Pike 225 

Tubbs, W. R. well. Hale 173 

Tubbs, Mr. B. and Mr. R. wells. Perry 181 

Tubbs, Reuben well. Dallas 202 

Tucker. Eton well r. Russell 233 

Tunstall, Wiley wells, r. Hale 168 

Tunnel Springs springs, a. Monroe 277 

Tunstall, Mrs. place well, Hale 170 

Turkey Creek Springs, Choctaw 293 

Turnipseed, Mrs. Sallie well, Pickens 128 

Turpiii, J. H. well. r. Hale 172 

Tuscaloosa City well, Tuscaloosa 98 

Tuskegee wells, Macon 222 

Tutwiler, Peyton wells, Perry 178 

Tyson, Silas wells, Montgomery 214 

Ullman place wells, Dallas ^ 202 

Underwood, Ike place wen, Terry 178 



a — analysis given, r — record given. 



382 Index. 

Union Slaughterhouse well, r. Montgomery 213 

Union Springs and vicinity wells, Bullock 228 

Union Springs City waterworks well, r. a. Bullock 228 

Uniontown and vicinity wells, Perry : 180 

University of Alabama spring, a. Tuscaloosa 116 

Upshaw Bros, well, Russell 236 

Upshaw, J. W. well, r. Russell 236 

Valhermoso springs, Lawrence 103 

Vandei"slice place wells, Perry 179 

Van Dorn Station well, Marengo 185 

Vaughn, Dave well, Wilcox 282 

Vaughn place well,. Perry 179 

Verner, Charles & King, Henry well, r. Tuscaloosa 120 

Vienna Baptist Church well, Pickens 126 

Vorn, W. W. well, r. Covington 261 

Wade place well, Dallas 203 

Wadsworth, Alt. well, Autauga 219 

Wadsworth, John well, r. Autauga 219 

Walker Springs, Choctaw 294 

Walker Springs, Clarke 286 

Walker place well, Pickens 127 

Walker, Mims well, Marengo 186 

Walker, C. D. wells, Marengo 186 

Walker, A. E. well, Hale 171 

Walker, J. N. well, Dallas 203 

Walker, A. B. well, Russell 234 

Wallace, R. B. wells, Perry 181 

Wallace, T. M. wells, Perry 177 

Waller, Lichtman & Murphy Land & Development Co. wells, 

r. a. Hale 161 

Ward, tract well, Dallas 203 

Warriorstand well, Macon 222 

Warsaw & Vicinity wells, Sumter 135 

Washington, Carter well, Hale , 173 

Washington, George well, Dallas 205 

Watt place well, Dallas 205 

Webb, Capt. James well, r. Greene 156 

Webb, John C. wells, r. Marengo 184 

Wedgworth Store well, Hale 164 

Wedgworth, W. M. wells, r. a. Hale 162, 163, 164 

Wedgworth (Greenwod, Mays Sta.) wells, Hale 163 

Wedgworth, C. H. well, r. Hale 163 

Wedgworth, W. E. wells, r. Hale 162, 164 

Welch plantation well, Dallas 198 

Welch, J. C. wells, Perry . 180 

Weston place well, Sumter 136 

White, T. A. well, r. Sumter 141 

White, R. A. well, Hale 173 

\vhite, Sallie well, Perry 182 

White, Judge W. R. well, Pike 225 

White, S. H. wells, Dallas 203 

Whitfield, Jesse wells, Marengo 1S5 



a — analysis given, r — record given. 



Index. 383 

Whitsitt & Vicinity wells. Hale 170 

Whitten, W. E. well, Pickens 130 

Wier, .Mrs. Peter wells. Sumter 130 

Wier, Win. well, r. Sumter 138 

Wiggins, 0. L. well, Escambia 272 

Wilder, Sam, wells, Pickens 125 

Wilder Place wells, Pickens 128 

Wilkins, J. F. (old) wells, Pickens 127 

Wilkins, Minge, (old) weds, Marengo 186 

Williams, L. W. well. Pike 225 

Williford's Landing well, a. Tuscaloosa 122 

Willis. Wm. well, Sumter 136 

Wilson. Mrs. well. Macon 223 

Wilson place wells, Dallas 200,204 

Wilson, Allen place wells, Hale 164 

Wyndham Place wells* Pickens 128 

Windsor Place wells. Marengo . 185 

Witherspoon's Spring, Lauderdale 103 

Wood place well, Dallas 206 

Woodruff place well, Dallas 202 

Wooley Springs, Limestone 102 

Wooten well. Marengo 189 

Wyndham Springs, Tuscaloosa 92 

Wyndham, Walter well, Pickens 129 



a — analysis given, r — record given. 



Autauga County. 215.219. 

Artesian prospects 215 

Wells described 216-17-18-19 

Shallow waters 215 

Barbour County. 238-244. 

Artesian prospects . 240 

Surface features 238 

Baldwin County. 314-316. 

Artesian prospects 316 

Mineral waters 316 

Shallow waters 315 

Surface features 314 

Bashi formation 17 

Bibb County, Appalachian division, 83 ; Coastal Plain division, 122. 
Bullock County. 226-229. 

Artesian prospects : 227 

Surface features . 226 

Butler County. 263-267. 

Artesian prospects 266 

Mineral waters 263 

Surface features . 263 

Cahaba field details i. , 94 

Cullman County 95 

Chattahoochee River drainage, "Blue Marl" region 230 

Chattahoochee Series 21 

Chickasaw Group 15 

Chilton County 123 

Choctaw County. 290-297. 

Artesian prospects 295 

Mineral extracts : 290 

Mineral springs '. 290 

Of the Biuirstone & Hatchetigbee formation 291 

Of the Claiborne formation 290 

Of the Naheola formation 295 

Of the Nanafalia formation 294 

Of Tuscahoma formation 294 

Of Woods Bluff formation 294 

Surface features 290 

Claiborne Group 17 

Clarke County. 283-289. 

Artesian prospects 284 

Mineral waters 283 

Surface features 283 

Clayton limestone 15 

Climate of Alabama , 25 

Coal fields, Geological characters •__ 9 

Details in ' 88 

Coastal Plain Division, geological characters, 12 ; general ac- 
count of, 108 ; arrangement of strata in, 61 ; details of 
waters in 108, 318, 320. 



Index. 385 

Coffee County. 256-258. 

Artesian prospects 256 

Surface features 256 

Conecuh (Yiunly. 2G7-2G8. 

Artesian prospects 268 

Surface features 267 

< Jorrections 321 

Covington County. 258-261. 

Artesian prospects 259 

Shallow waters 258 

Surface features 258 

Crenshaw County. 261-2G3. 

Artesian prospects 261 

Surface features 261 

Cretaceous, Geological characters of, 13 ; Details of Water 

Resources of. 111, 318. 
Dale County. 255-256. 

Artesian prospects 255 

Dallas County. 190-206. • 

Artesian records 192 

General conditions 190 

Decline and failure of Artesian wells 62 

Deep-seated waters 51 

Deep springs , 51 

Deep zone of flow of underground waters 46 

Depth of penetration of underground waters 36 

Discussion by counties— Cretaceous 111 

Discussion by counties — Tertiary 245 

Disposition of water falling upon land surface 32 

Direct runoff or flood flow 33 

Distribution and movement of underground waters 37 

Driven wells, recovery of water by 49 

Effects of erosion on artesian wells 57 

Elmore County. 219-221. 

Artesian conditions 220 

Shallow waters 219 

Surface features 219 

Eocene formations 14 

Escambia County. 2G8-275. 

Artesian prospects 2G9 

Surface features 268 

Essential conditions of artesian wells 52 

Etowah County 93,94 

Fayette County, Appalachian Division, 97 ; Coastal Plain Division, 114 

Final runoff, underground water 35 

Fog __J 29 

Form of underground water table 44 

Frost 26 

General discussion underground waters 32 

Geneva County. 254-255. 

Surface features 254 

Artesian prospects 254 

Geographic position of Alabama 1 

Geology of Alabama, general account of 4 

Gosport greensand 18 

Grand Gulf formation, Geological characters, 22 ; special topo- 
graphic and other features of, 248 to 251. 



386 Index. 

Greene County. 143-157. 

Surface features : 143 

Artesian records 145 

Ground water, division of 43 

Ground water movements, modification of due to stratification 40 

Ground water, modification of movements of 37 

Ground water movements modified by topography 43 

Ground water table, form of 44 

Hail 29 

Hale County. 15S-176, 318. 

Surface features 15S 

Artesian wells , 158 

Hatchetigbee formation 17 

Henry County 252 

Surface features . 252 

Artesian records 252 

Houston County. 252-253. 

Surface featui*es 252 

Artesian records 253 

Incomplete saturation by underground waters 39 

Jefferson County 96 

Lafayette formation 24 

Lamar County. 113-114. 

Artesian prospects . 114 

Shallow waters ' 113 

Later formations of Coastal Plain 25 

Lee County. 223-224. 

Artesian prospects 223 

Surface features 223 

Lisbon formation 18 

Lost water 39 

Lowndes County. 206-208. 

Artesian records 207 

Surface features . 206 

Macon County. 221-223. 

Artesian prospects 221 

Surface features _; 221 

Marengo County. 182-190. 

Artesian records 183 

Surface features 182 

Marion County 96 

Midway group 15 

Mineral ingredients in Artesian water 64 

Mineral waters, Appalachian Division. 

Talladega Mountain & Ashland Plateau 67 

Appalachian valleys 71 

Coal Measures 88 

Valley of Tennessee 101 

Miocene formations 21 

Modifying conditions in artesian wells 57 

Mobile County. 302-314. 

Artesian prospects 307 

Mineral waters 304 

Surface features 302 

Mobley, Judge, list of Greene County wells 146 



Index. 387 

Monroe County. 270-279. 

Artesian prospects 277 

Mineral waters 270 

Surface features 270 

Montgomery County. 208-214. 

Artesian records 20S 

Shallow waters 208 

Surface features •__ 208 

Mountain and table-lands, general discussion 3 

Nanafalia formation If! 

Naheola formation 15 

Open wells, discussion concerning 49 

Pascagoula formation 21 

Permeability of rocks 40 

Perry County. 17G-182. 

Artesian wells 177 

In Eutaw formation 178 

In Selnia Chalk — * 179 

In Tuscaloosa formation 177 

Shallow waters 170 

Physical Geography, Geology, and Climate 1 

Physical Geography and natural divisions 1 

Pickens County. 123-130. 

Wells in Eutaw formation, 124 ; in Selma Chalk, 128. 
Pike County. 224-220. 

Artesian prospects 224 

Pliocene formations 21 

Porosity of rocks 37 

Precipitation 28 

Quaternary formations 24 

Recovery of underground waters 48 

River systems in Alabama, general discussion 2 

Russell' County. 232-238. 

Artesian records 232 

Surface features 232 

Sucarnochee clay 15 

Saline waters; Appalachian Valleys, 82; in chemical discussion. 232 

Source of circulating waters 32 

Springs deep (fissure Springs) : 51 

Springs, recovery of water by 48 

St. Stephens Limestone It 

Sulphur and chalybeate waters Appalachian Valleys 73 

Sulphur Springs Valley of the Tennessee 101 

Sumter County. 131-143, 370. 

Artesian prospects 135 

Shallow waters 131 

Surface features 131 

Supplementary notes 317 

Surface configuration and grand division of Alabama 1 

Surface zone of flow in underground waters 44 

Tables of chemical analyses of Alabama waters .. 351 

Talladega Mountains and Ashland Plateau, Geology, 0. 
Details of underground waters in 00. 

Tar Springs in Valley of the Tennessee 104 

Temperature of Alabama ; climatic discussion 20 

Of artesian well waters 03 



388 Index, 

Tertiary, geological characters of, 14 ; Details of Water Re- 
sources of, 245, 320. 

Thunderstorms in Alabama ; climatic discussion 29 

Tuscaloosa County, Appalachian division 97 

Tuscaloosa County- — Coastal Plain division. 115-122. 

Artesian prospects 117 

Shallow waters 115 

Surface features 115 

Underground waters : cause and rate of movement of, 40 ; de- 
tailed description of in Alabama, G6 ; distribution & move- 
ments of, 37 ; general discussion of, 32 ; movements of 
modified by physical structure, 37 ; by stratification, 46 ; 
by topography, 43 ; recovery of, 48 ; source of, 32. 
Valley of the Tennessee, Geological characters, 10. 

Details of underground waters in 100,317 

Variations in the confining impervious beds 5i> 

Variation in water-bearing stratum : 58 

Velocity of movement of undergi'ound waters 41 

Walker County 94 

Warrior field, artesian prospects in 94 

Washington County. 297-302. 

Artesian prospects 300 

Mineral Springs 298 

Of the Grand Gulf formation : 299 

Of the Hatchetigbee formation 198 

Surface features 297 

Water, amount available to artesian wells 35 

Waters of the Cretaceous Hi 

Of the Tertiary : 245 

Wilcox County. 279-2S2. 

Artesian prospects 282 

Mineral waters 280 

Surface features 279 

Winds _- - 30 



MAY 181907 



IIBIIIMI«™ 0F CONGRESS 



020 108 539 1 



